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are reasons for disciplinary action and may 
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The 


Kentucky Geological 
Survey 


WILLARD ROUSE JILLSON 
DIRECTOR anp STATE GEOLOGIST 





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VoLUME TEN 
Geology of the 
Princeton Quadrangle 


1923 












(PROVIDENCE) sar 





BE FARMERSVILLE 














LEWISTOWN 























| OUTLINE MAP pie Se 23 sks = | PRINCETON 





| SHO , eel QUADRANGLE 
| SUE U STE E ELES Gre Lire ———-——-—-— _ STATE OF KENTUCKY 
| pu Peer es RAILROADS * ; = J Ly 





SKETCH MAP SHOWING FAULTS OF THE PRINCETON 
QUADRANGLE IN THE STATE OF KENTUCKY. 


The irregular lines which are numbered to correspond to the text rep- 
resent the surface extension of the faults. These lines will be easily 
distinguished from the North-South and East-West lines of longitude and 
latitude. This outline map is a reduced reproduction of the new stand- 
ard U. S. G. S. quadrangle (Princeton), scale 1-62,500, on which the areal 
and structural geology of this region has been plotted by the author, 












(DAWSON _SPRINGS 











(GEOLOGY of the 
PRINCETON QUADRANGLE : 


A Detailed Report on the Stratigraphy 
and Structure of the Princeton, 


Kentucky Region 





BY 


STUART WELLER 


ASSISTANT GEOLOGIST 


Presented With Four Separate Miscellaneous Papers 
BY 
ArtTHur McQuiston MILLER 
WILBUR GREELEY BURROUGHS 


ADOLPH CHARLES NOE and 
WILLARD ROUSE JIILSON 


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5 a I SNR ALY . 
Illustrated with forty-two Photographs, ~~ ~'5 HAR oF The 
Maps and Diagrams FP aa 
: 
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First EDITION ee LNULS 


500 CopPIEs 


THE Kentucky GEOLOGICAL SURVEY 
FRANKFORT, Ky. 
1923 


THE STATE JOURNAL COMP 


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Printer to the Commonwealth 


Frankfort, Kentucky. 


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Letter of Transmittal 


Dr. W. BR. JILLSON, 
Director and State Geologist, 
The Kentucky Geological Survey, 
Frankfort, Kentucky. 


DEAR SIR :— 


I am transmitting herewith the manuscript of a report on 
the stratigraphie and structural Geology of the Princeton Quad- 


rangle of the United States Geological Survey topographie atlas. 


This is the second quadrangle lying within the highly faulted 
area of western Kentucky which includes the important fluorspar 
deposits of the State, upon which I have reported. The first 
of these reports was upon the Goleonda Quadrangle; and a third 
upon the Cave in Rock Quadrangle, including most of the 1m- 
portant mining area of Crittenden County, will be made later. 
Nearly the whole of the area covered in the present report is 
included in Caldwell County. The careful and accurate mapping 
of the structure and stratigraphy of these areas will undoubtedly 
prove to be of very great assistance in further prospecting and 
development in the Western Kentucky fluorspar field. 


Respectfully submitted, 


STUART WELLER. 
The University of Chicago, 
Chicago, III. 
Oct. 1st; 1922. 


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Contents 


Letter of Transmittal: Geology of Princeton Quad- 


Vv 


89 


93 
97 
oo 


127 


PAD SLOT ey A eae sea eo Ran oie ee ere ne 
Contents ‘fins Se a Se ce ee eee 
Hlustrations =... NS cil et Deas Sete he oe a as Re 
I. Geology of the Princeton Quadrangle, Ky., ‘by 

Stuart Weller: 
Chapter oe INtroduehio ny cece ee eee 
Chapter IL Stratigraphic -Geology. 22.252 
Chapter III. Stratigraphic Geology, Iowa Series 
Chapter IV. Stratigraphic Geology, Chester 
OTIOS <2 sees sc last ee hee oe eee cee eee 
Chapter V. Stratigraphic Geology, Pennsyl- 
VanlaneSystemMn.2. eee eee ee 
Chapter VI. Stratigraphic Geology, Lafayette 
GEV OL reared ea eae eee eee tee 
Chapter Vilv -l2neéous: Rocks 2. oe eee 
Chapter. VUT.- Structural’ Geology. 2... 
II. Recent Cave Explorations in Kentucky for Animal 
and Human Remains, by Arthur McQuiston Miller 107 
Ill. A Pottsville-Filled Channel in the Mississippian, 
by Wilbur, -Gréeley..Burroushse 2). ee 
IV. The Flora of the Western Kentucky Coal Field, by 
Adolph Charless NGOs Cees. o te ee eee 
V. A Bibliography of the Mammoth Cave of Kentucky, 


Dy: “Willard. Rousesillsone 2 ee eee 


Td ex eee Pe cece ee ae ee 


ConA Ma ww Ss 


DNONDDNDNYNNNHHH HHH PH pp 
PABA HN ER SSCHONAMTR WN ES 


35. 
36. 
37. 
38. 
39. 
40. 
41. 
42. 


Illustrations 


Page 
Frontispiece: Sketch Map Princeton Quadrangle........................ ii 
ORL ILD TE PIMCOLOM see Hoy oy FUCLLOD ey see oe ete ea aeoe tan Os teehee 2 
Metal ote FardinSDuUres SAlLdStONG oc tence oF es et ae ee, 6 
PUI RGmL OCA Le DGLOTINA GION a scents cosesessvulcecssicowdesopeste coco Sines ate geaatt an 10 
P ATIGUGTN GT OLmA VV ALOIE G5 God) Gr eee ta cet oan oe eect eT oR we 21 
AD Debate GLtlon wl UIFt Sy DEIN ES ATL OSUOM Case tee oon ccc the ans cicc¥enceasise 27 
PIGCATEPOUR Tr Cll Ube adn CSLON CG wage tasers geen ces ces sree oe ete rc nce 33 
PerUneustel all-in the Deg Gls SANSOM C Merc. .c.-cccaeeeree st tan tee ceacecoee 41 
Steeulveincuneds Cy Press xsaNas tO ec. cecs sence ok ere dee vi cece 53 
Pwetorerons Ofs Lie. .Glen ss Dea reese ccesor eo easren coc ett ae snnce eee eee 64 
ha somU ree! Ate PLINgS = OAD CSCO LH Cet! ce nce tree ce eee She he pete cata cere 67 
PUGeLriincaling PireCtsa OL. cEilOSl OM) uke. cscs tre preg eee eet evan zee coe 72 
Panoramic Section, Walche’s:Cut. (tipped: 1n)= 2-2... 222k a. 100 
Hines’ Cave, Near Mill Springs, Wayne Co., Ky. ..................-2--+- 110 
PHOIANS SICICLON SIN ee ULAA Le OSI EL ONT sor teneipiees bec dece on ccuk te cneuwacstte sees ie 
HPectlioneGieLOoLavilost 1 led) Channels kel ain eee sateen 118 
Diagrammatic Section of Faulted Pottsville Filled Channel...... 120 
Coa balletroni West. hentuckye Mine NO: 12 ‘2.c:dcctiveeitsaccssstoteee 127 
Ideal Coal-Measure Swamp in Kentucky  -0.0.2.....0..ceccceeeeseeeceeecceeeeeee 128 
Lepidodendron Volkmannianum from Princeton, Ky. .................. 129 
Lepidodendron Volkmannianum from Princeton, Ky. .................. 130 
Lepidodendron Veltheimianum from Princeton, Ky. .................. 131 
Lepidodendron Veltheimianum from Princeton, Ky. .................. 131 
Pe DIOOUCHO LOM OMe TINCELON Ss -  Vioe yc. seeet soci seers eo recsesnck eotn ey ones 132 
Decorticated Lepidodendron Stem from Princeton, Ky. ........ eo 
Decorticated Lepidodendron Stem from Provindence, Ky. ........ 134 
Decorticated Lepidodendron Stem from Princeton, Ky. .............. 135 
Transverse Cut of Branching Lepidodendron Stem from Coal 
NSSOUD DE oS ckeerd Bale aR ta Mra WES te Alen fay ate US pte Nate Pins ea NN ince ae On ar 136 
Lepidodendron Leaves from Princeton, Ky. -......0.....cc.ceccccee eeeeeee eee 137 
Sip iiiaride Lomntrom marlin ge tons. Var ee ies ae, eee 137 
SLicmarigal 1 COldGS = frOM HeENdersoOMny, WS Vivv.s---ccscesce ete esces eee 138 
Calaihices -SUCKOVIE from» Erin Geton, \KiVare eee... secceseceesc ers eee 139 
Annularia Sphenophylloides from Braidwood, Ill. ........00.000....0002.. 140 
Sphenophyllum Emarginatum from West Kentucky Mine 
TED Wi aPaaplen ce iat ES Seana et hoa ah POE A Ran CO <<. ORR ck SC REA 141 
Sphenophyllum Emarginatum from Braidwood, IIl. .................. 142 
Sphenophyllum Stem in Transverse Section from Coal Ball ...... 143 
Menropteris) Leaves, frome MOOrman SK yc 5 iscstecsde sche cesses te esas iticccee 144 
Neuropteris Rarinervis from Spring Valley, IIl. ........0000... 145 
PUVSORLOMA, SCCC sLrOMeppring  VaLLGY, sLile ens ee ieee 146 
Lagenostoma Seed in Longitudinal Cut from Coal Ball............ 147 
(ordaitegsirom wWest-Kentucky= Mingo NOiv 6.2 cocci ee ce 148 


Outline Map Princeton Quadrangle Showing Fault Pattern. 
Scale 1 in=-1 mile, by Stuart Weller (Separate, inside back cover) 








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GEOLOGY of the 
PRINCETON QUADRANGLE 





I. 


GEOLOGY of the PRINCETON (QUADRANGLE 
By STUART WELLER, Assistant Geologist 


CHAPTER I. 
INTRODUCTION 


The Princeton Quadrangle of the United States Geological 
Survey Atlas of topography, Hes between longitude 87° 45’ 
and 88°, and between latitude 37° and 37° 15’. It covers about 
240 square miles, all but about 22 miles of which is included in 
Caldwell County. The smaller portion, in the southwestern 
corner of the quadrangle, lies in Lyon County. 


Nearly the entire of the area is extensively faulted. The most 
complicated faulting lies along a belt extending in a northwest 
direction from a little south of Claxton, near the eastern border 
of the quadrangle, to the western border about two and one-half 
miles south of the northwestern corner. Apart from the fault- 
ing in this belt, where the direction of individual faults is 
in nearly every point of the compass, the major faults are for the 
most part in a general east-west direction. None of this faulting 
is reflected to any great extent in the topography of the area. 
In places drainage lines have been developed along fault lines, 
and after the structure is worked out, the faults are found 
locally to follow ravines and gullies in many places, but there 
are no outstanding topographic characteristics which would 
suggest to the observer of the topographic may alone that the 
area is complexly faulted. The southwestern ‘portion of the 
_ area, about one-fourth or a little more of the whole, is rather 
sharply differentiated topographically from most of the remain- 
ing part of the quadrangle, by reason of the presence of great 
numbers of sink holes. These sinks are largely characteristic 
of the Ste. Genevieve limestone. Aside from the sink hole area 
the topography is essentially mature in its stage of development, 
being fully dissected. In places where the less resistant lime- 
stone and shale beds constitute the surface formations, the 
topographic expression is somewhat soft, but elsewhere it is 
decidedly rugged. 


2 PRINCETON QUADRANGLE 








The town of Princeton, with about 3,689 inhabitants, is 
the County Seat of Caldwell County, and is situated near the 
eenter of the Quadrangle. A number of other villages, consist- 
ing of one or more stores and a few houses, are scattered through 
the area. Of these Crider, Farmersville, Cedar Hill are per- 
haps the most important. Smaller villages are Flat Rock, Rufus, 
Lewistown, Olney, Claxton, Dulany, Scottsburg, MeGowan, 
‘Otter Pond, and Saratoga. 

Nearly the entire area is drained by comparatively small 
streams. Tradewater River crosses the northwestern corner of 
the Quadrangle, and approximately one-half of the entire quad- 
rangle drains into this stream through Flynn and Donaldson 
Creeks and their tributaries. The more southern portion of the 
area, separated by an irregular, northwest-southeast line, fol- 
lowing in the main the southern border of the more faulted 
belt, drains into the Cumberland River through Eddy Creek 
and its tributaries, and White Sulphur Creek. 


G Va 


i Marion 


4 


/ 


SalemO 





, Sketch map of a portion of .Western Kentucky and Illinois showing the 
geographical position of the Princeton Quadrangle. The white area is 
Mississippian except west of the Tennessee River. Coal, Measures cover 
the stippled areas. Ps 


INTRODUCTION 


ee] 








In the State of Kentucky it is much more difficult to 
describe the exact location of specific points, than in the states 
where the federal land surveys have subdivided the surface 
into townships and sections. Where these subdivisions have 
been made it is a simple matter to describe the location of a 
given point within the limits of a 40-acre tract, or even within 
the limits of a 10-acre tract. . This cannot be done where such 
land surveys do not exist. The Kentucky quadrangles are 
divided, however, into nine smaller quadrangular areas by the 5- 
minute lines of longitude and latitude, and for the purpose of 
assisting in describing locations, some nomenclature of these 
smaller quadrangles is convenient. In the present report these 
smaller units will be designated as rectangles to distinguish 
them from the quadrangle as a whole, and each will be desig- 
nated by the name of some geographic feature present in that 
particular unit. Beginning at the northeast corner of the quad- 
rangle map, the rectangles will be designated as follows: first, 
the Tradewater rectangle, so-called from the presence of the 
river of that name, which does not enter any other rectangle 
on the map; second, next west of the Tradewater is the Farm- 
ersville rectangle; third, next west of the last is the Flat Rock 
rectangle; fourth, south of the last is the Crider rectangle, to 
the east of which; fifth, is the Princeton rectangle; sixth, east 
of the Princeton is the Claxton rectangle; seventh, south of the 
Claxton is the Otter Pond rectangle; eighth, west of the Otter 
Pond is the McGowan rectangle; and ninth, west of the 
McGowan, in the southwest corner of the map, is the Saratoga 
rectangle. | 


The field work upon which this report is based was carried 
on throughout the whole of the 1921 field season, and during a 
part of 1922. In the prosecution of the work the writer has 
been most efficiently assisted by Mr. Ben B. Cox. The same 
assistant has also rendered great service in his study, under 
the writer’s direction, of the fossil collections, from the region, 
and in the compilation of the several lists of fossils which are | 
included in the report. For the identification of the fossil 


4 PRINCETON QUADRANGLE 


bryozoans in the several faunas, acknowledgment is due Mr. 
A. C. MeFarlan, who has been engaged for a number of years 
in a very detailed study of the bryozoans of the Chester faunas. 
Throughout the progress of the work Dr. Jillson, Director of the 
Kentucky Geological Survey, has done much to facilitate the 


investigation. | aS 


CHAPTER II. 


STRATIGRAPHIC GEOLOGY, FORMATIONS NOT 
EXPOSED AT THE SURFACE 


INTRODUCTION 


The hard rock geologic formations which are exposed at 
the surface in the Princeton quadrangle are all Mississippian 
and Pennsylvanian in age. The oldest exposed formation is the 
Spergen or Salem limestone, whose position is somewhat above 
the middle of the Lower Mississippian or Iowa Series. The 
remaining higher units of the Iowa Series are all well exhibited 
within the quadrangle, and also the whole of the Upper Missis- 
Sippian or Chester Series. The Pennsylvanian is represented 
only by strata of Pottsville age. 

Although no formations older than the Spergen or Salem 
limestone are exposed at the surface, the succession of beds down 
to and including some portion of the Devonian, has been made 
known by the drilling of a deep well near Cedar Hill, on the 
farm of Mrs. W. F. O’Hara. This well was drilled during 
the vear 1921, and a fairly complete series of cuttings from the 
different depths has been preserved by Mr. F. K. Wylie, of 
Princeton. These cuttings have been generously placed in the 
hands of the writer, who is under great obligation to Mr. Wylie 
for the privilege of studving them. The depth of the well is 
2,017 feet, and the strata penetrated are as follows: 


Log of Well at Cedar Hill, Kentucky 


Iowa Series (Lower Mississippian) Thickness. Depth. 
PiOreE SEL TTD LON tua 1 thee Oe ei oe ered eae Re 250 250 
Gray limestone, more or less crystalline, with 

“SACS? CCA RE Be ieee Heth ee Rete ices eens ae 5 255 
PORTERS SLITS) LO Sees ec tia, Labs ae a ee eget eee tee 55 310 
Dark and light gray limestone, more or less 

erratallinegss wills chertesse:. 225 foe 240 550 
Black Silico-caleareous shale 2.2..242.22n.....22-4 10 560 
Dark, silico-calcareous shale with some gray 

NST OVEN RA) 003 ghee ve eee ie ie At SY Fas es oe oe 25 585 
Brown limestone with chert and pyrite ............ 65 650 
Brown to gray limestone with chert and pyrite 30 680 


Gray and brown limestone with chert and 
RATS Rl De he Aiea mops = Ae ave ec ee er are ey pec 350 1030 


6 PRINCETON QUADRANGLE 


Brown limestone with some silico-calcareous 


shale, some (cherteandepyrite io ee 70 1100 
Dark to black silico-calcareous shale with some 

Dyrites# NOjACheGih teak ee ee 502 1602 
Black, silico-calcareous shale, more siliceous 

than-a@bOvenrs twee eek ee eee ee 8 LOLe 
Black, silico-calcareous shale with some gray 

Limestone eee ee ee ent en ee ee 5 1615 
Greenish black, highly siliceous shale ................ 10 1625 
IN Cee AI ro os ee nas esac ee Oa ae ee, Se ae 5 1630 

Chattanooga Shale (Devonian) 

Brown to black shale with Sporangites .............. 135 1765 
Black siliceous shale with conspicuous pyrite 

Hedsat 183 seen ae ee Lo ree 107 1872 

Devonian Limestone 

White crystalline limestone 22.2.5 10 1882 
rray chert with some white limestone .............. Bye] 1915 
No sain phe". ee URE ere oe at eee. O55 2010 
White to dark gray limestone with some chert. 

Kraementvol Mavosites =<. .-<ccee cree ee 2010 
White crystalline limestone with some darker 

TPASMCIUG eh cn a ed ee eee 2017 


The top of the well is at an elevation of approximately 490 
feet above sea level. In the Cedar Hill quarry, about one-half 
mile northeast of the well, the contact between the Ste. Gene- 





TT Te 


. DETAIL OF HARDINSBURG SANDSTONE. Lay 


ro 'Shaly Hiardinsburg Sandstone, Walche’s Cut, Illinois Central Railroad, 
east of Scottsburg. 


STRATIGRAPHIC GEOLOGY—SURFACE FORMATIONS z( 


—— 





vieve limestone, the uppermost formation of the Lower Mississip- 
pian or Iowa Series, with the overlying Renault limestone of the: 
Chester Series, is at an elevation of 500 feet, a difference of ‘6 
feet. However, the interval between the top of the well and the 
top of the Ste. Genevieve limestone is somewhat greater than 
this because of the gentle dip of the beds to the northeast, and 
it is assumed that 70 feet of Ste. Genevieve limestone should 
be present above the ground at the location of the well. This 
thickness, added to 1,630 feet, the depth of the well to the top 
of the Chattanooga shale, gives a thickness of 1,700 feet for the 
entire Iowa Series, which is considerably greater than has been 
recorded in the Ohio and Mississippi Valleys. 
In the typical section of the Iowa Series as exhibited in the 

Mississippi Valley, the following formations are recognized: 

Ste. Genevieve limestone. 

St. Louis limestone. 

Spergen or Salem limestone. 

Warsaw limestone and shale. 

Keokuk limestone. 


Burlington limestone. 
Kinderhook Group. 


In the Cedar Hill well section it is not possible to draw any 
sharp lines of demarkation between the several units of the 
typical section, although the three uppermost formations are 
distinetly recognizable in the surface outcrops. The nearest 
area in which these lower formations are exposed at the surface 
is in Hardin County, Hlinois, about the Hicks dome, but the 
Cedar fill section is considerably greater than the estimated 
thicknesses of the several recognized units in Hardin County, 
but, as might be expected, the lithology is perhaps somewhat 
moie like that of Hardin County than that of the more typical 
Mississippi River section. | ae j 
PORN, Pas oh te: 


DEVONIAN 


Devonian Limestone. The Cedar Hill well penetrates to a 
depth of:2;017 feet, the lower 145 feet being in beds beneath the 
Chattanooga shale. So far as samples: have been saved,.:the 
whole of this is a, limestone formation, that portion between - 


8 PRINCETON QUADRANGLE 
1882 and 1915 being largely a gray chert with a lesser amount of 
white limestone. Samples from other beds show that the lime- 
stone is prevailingly hght colored, much of it very white and 
crystalline. The sample from the depth 2,010 is somewhat 
darker than the others, being a mixture of white limestone and 
darker gray limestone with some chert. At the bottom of the 
well the limestone is again lighter in color. The position of this 
limestone directly beneath the Chattanooga shale suggests that 
its age is equivalent to that of the limestones which lie beneath 
that formation elsewhere in the Ohio Valley. The contact 
between the Chattanooga shale and the underlying limestone 
is exposed at the surface in southern Ohio and Indiana, in 
Kentucky south from Louisville and elsewhere, in Hardin 
County, Illinois, and again in Union County, Illinois, near the 
Mississippi river. Wherever this contact is known the sub- 
jacent formation is a limestone of Middle Devonian age, and 
in all probability the lmestone in the Cedar Hill well is of 
the same age. A more exact correlation cannot be attempted 
with the available data. In one of the well samples, at the 
depth of 2,010 feet, a fragment of a species of the coral genus 
Favosites has been detected, and while this is not conclusive, 
it is in full harmony with the Middle Devonian age of the bed. 
Chattanooga Shale. One of the most persistent formations 
throughout the Ohio Valley, extending northward in Ohio, 
Indiana and Illinois, southward along the Appalachians, and 
westward as far as Oklahoma, is the Chattanooga shale. The 
formation has been deseribed under various names!, but wher- 
ever the proper portion of the geologic column outcrops, the 
shale oceurs. It is also uniformly met with throughout this 
area, in wells, where younger formations are present at the 
surface. The formation is very uniform in its lthologie char- 
acters, being a dark brown or black, fissile shale, with hard 
layers or lenses in places, which are likely to be more or less 
charged with pyrite. A very characteristic feature of the shale 
is the presence, in greater or less abundance, of the empty spore 
cases of an extinct plant, called Sporangites. These little bodies 
are circular and disk-like in form, of small size, being only a 
fraction of a millimeter in diameter, and brown or resinous in 


1See Ill. State Geol. Surv., Bull. No. 4], p. 87 (1921). 


STRATIGRAPHIC GEOLOGY—SURFACE FORMATIONS 9 


_—— 





eolor and appearance. These characteristic sporangites are 
present in some of the chips taken from the Cedar Hill well, 
and the lithologic character of the chips corresponds with that 
of the surface exposures of the formation. 

The thickness of the Chattanooga shale in the Cedar Hill well 
is 242 feet, which is considerably greater than has been recorded 
elsewhere in Kentucky. In Jefferson County Butts reports a 
thickness of 100 feet.2, In a number of wells in Warren County 
the thickness of the black shale varies from 21 to 185 feet, while 
in Allen County the thickness is commonly between 40 and 50 
feet, although extremes of 9 and 116 feet are reported.* The 
thickness of the shale in the Cedar Hill well is less, however, 
than has been reported from Hardin County, Illinois, where 
the formation has an estimated thickness of 400 feet.* 


MISSISSIPPIAN 


The lower formational units of the typical Iowa Series of 
the Mississippian cannot be fully differentiated as such, in the 
Cedar Hill well. Lying just above the Chattanooga shale there 
is a black to greenish, highly siliceous shale bed, probably 15 
feet in thickness, above this for five feet there are some frag- 
ments of gray limestone in the drill cuttings, associated with 
black, silico-caleareous shale. Overlying these lower beds there 
is a little more than 500 feet of dark, mostly black, silico-cal- 
careous shales. Throughout this thickness the fragments pre- 
sent in the well samples effervesce freely in hydrocloriec acid, 
but leave a large insoluble residue, some part of which seems 
to be fine siliceous grains. The fragments in the samples of 
cuttings are more or less flake-like, resembling shale. These 
beds probably cannot be considered as limestone, although a 
considerable proportion of calcium carbonate is present, but 
rather as a calcareous and siliceous shale. The bed might also 
be looked upon as an impure, siliceous limestone. Lithologically 
these beds are conspicuously different from any of the Kinder- 
hook, Burlington and Keokuk strata of the typical section, 
although their position would indicate their equivalence with 


ae 


Zi ve, Geol Surve, cers 4, 5V 01.) 0.) pt. 2, p.. 1380 (C1915): 
BIC Ve GeCOlaoluLy se selwn Om, DULL eNoe 1, PDy 179-191 and 504-516 (1920). 
Slime State: Geol, Sury., Bull. Now 41, 1p. 92. (1921): 





10 PRINCETON QUADRANGLE 


these lower formations of the Iowa Series. These beds perhaps 
resemble more closely that portion of the Mississippian section 
in Hardin County, Illinois, which has been referred to the 
Osage.” The Osage in Hardin County is poorly exposed, being 





INTENSE LOCAL DEFORMATION, 


These greatly contorted beds of Paint Creek Limestone adjacent to 
the main fault in Walche’s Cut, indicate to what degree the original bed- 
Ging of the sediments of the Princeton Quadrangle has been altered. 
The significance of such a degree of deformation is at once apparent. 


represented almost entirely by broken residual chert upon the 
surface. Some portions of the chert resemble a fine grained 
sandstone, and originally may have been a siliceous limestone 
in which the silica occurred in the form of very fine quartz 
erains. The chert in Hardin County is believed to be only a 
superficial development at or near the surface, and the formation 
may be much like that in the Cedar Hill well where it is deeply 
buried. The computed thickness of these beds in Hardin 
County is 550 feet, which compares favorably with the thickness 
present in the Cedar Hill well. 

Overlying the dark, impure limestone or silico-caleareous 
shale which possibly represents the Osage division of the lowa 
Series, the Cedar Hill well samples are essentially all lime- 
stones, from brown to light and dark gray in color, and most of 


oT Srate Geol nsuiny. eb Ulli ONO Ale poz Ole 


STRATIGRAPHIC GEOLOGY—SURFACE FORMATIONS 11 





them include numerous fragments of chert, so that the entire 
thickness of strata, down to the depth of 1,100 feet, seems to 
have been a series of more or less cherty limestones. If the 
beds below these lmestones are equivalent of the Osage, then 
these cherty limestones are the equivalents of the Warsaw, 
Spergen or Salem, St. Louis, and Ste. Genevieve limestone for- 
mations. The three higher units mentioned are exposed at the 
surface within the Princeton Quadrangle, the St. Louis and 
Ste. Genevieve limestones being extensively exposed. None of the 
samples of cuttings from the well seem to have been taken from 
the Ste. Genevieve limestone, but the first sample was taken at 
a depth of 250 feet, which would permit a thickness of over 
300 feet for that formation, which is the estimated thickness 
in this general region. The drill cuttings from the lesser depths 
of the well, that have been saved, are of a lithologic character 
to be expected from the St. Louis limestone, but the basal limits 
of the formation cannot be established. If a thickness of 350 
feet be allowed for the St. Louis, added to approximately 250 
feet of Ste. Genevieve limestone, a thickness of 500 feet remains 
between these beds and top of the silico-calareous shale or impure 
limestone which sets in at about 1100 feet, such a thickness is 
greatly in excess of any observed thickness of the Spergen and 
Warsaw formations, these beds being estimated at. 250 feet in 
Hardin County, Illinois.© In all probability the St. Louis 
limestone in the section is considerably thicker than the sug- 
gested 350 feet, perhaps as much as 500 feet, but there is no 
evidence afforded by the samples of drill cuttings whereby the 
base of the St. Louis limestone can be certainly fixed, nor is there 
any basis for the identification of the Spergen or Salem lime- 
stone, although the equivalents of these formations must be 
present in the section. 


*¢ill. State Geol. Surv., Bull. No. 41; p, 99 (1921). 





CHAPTER III. 
STRATIGRAPHIC GEOLOGY, IOWA SERIES. 


Introductory Statement. The hard rock formations: 
exposed at the surface within the Princeton quadrangle are 
all Mississippian and Pennsylvanian in age. The oldest of the 
exposed formations is the Spergen or Salem lmestone, the’ 
youngest one being of Pottsville age, in the lower Pennsyl- 
vanian. In addition to these, however, a formation consisting 
of unconsolidated gravel, probably of late Tertiary age, caps 
some of the high hills in the western and southwestern portion 
of the quadrangle. The several formations will be considered 
in order, beginning with the oldest one. 

The formations of the Mississippian System are divisible 
into two series, which have been referred to many times in the 
literature as Lower and Upper Mississippian. The Upper’ 
Mississippian has long been known as the Chester formation or 
croup, but the investigations of recent years have shown that 
the Chester is deserving to rank as a distinct Series, made up 
of many different formations. The Lower Mississippian has 
long been subdivided into a number of more or less well defined’ 
formations, but only recently has there been a distinct Series 
name applied to the whole succession of formations, the name 
so used being the lowa Series,! adopted because the more typical 
section of the series is exposed in the southeastern portion of 
that state, and in the adjacent portions of Illinois and Missouri, 
and because the section was first worked out in detail by James’ 
Hall during his work as State Geologist of Iowa. 

The fowa Series is subdivided into the Kinderhook, the 
Osage, and the Meramee Groups, formations of the last of these: 
groups only being exposed within the limits of the Princeton 
Quadrangle. 


SPERGEN OR SALEM LIMESTONE 


Name. ‘The early collectors of fossils in Indiana discovered 
a locality near Salem, in Washington County, where great num- 
bers of small fossils occurred in an oolitic limestone. This 
locality came to be known as Spergen Hill or Spurgeon’s Hill 








avener, Jour, Geol., Vol. 28, "pe 282 (1920); 


14 PRINCETON QUADRANGLE 





by the local collectors, doubtless from the name of the property 
owner of the locality, pat the name never has had any standing 
as a recognized geographic term, and is not to be found upon 
any map. The fossils from this locality came to be known as 
the Spergen Hill fauna, but were always referred to either the 
Warsaw or the St. Louis formation. Spergen Hill or Spergen 
was never used as a true formation name until it was proposed 
by Ulrich. In 1897 Hopkins and Siebenthal ? published a report 
on ‘‘The Bedford Oolitic Limestone of Indiana,’’? in which 
they proposed to use the name Bedford limestone for the for- 
mation in question. It has been shown by Prosser,® however, 
that the name Bedford had been applied by Newberry in 1870 
to one of the geological subdivisions in Ohio, and consequently 
was preoccupied at the time it was proposed by Hopkins and 
Siebenthal for this Indiana formation. Siebenthal+ later 
claimed that the name Bedford had been used for the Indiana 
formation as early as 1862 by Richard Owen, but it seems clear 
that Owen’s use of the name was not intended as a formation 
name as such names are now used. In 1901 Cumings® proposed 
to substitute the name Salem for the Indiana formation inelud- 
ing the Bedford building stone, and with the elimination of 
Bedford because of its prior use in Ohio, this seems to be the 
first legitimate name given to the formation. In 1904 Ulrich & 
first applied the name Spergen Hill limestone to the formation, 
this name being exactly equivalent to the Salem limestone of 
Cumings. In 1905 Ulrich’ again used the name in the same 
Sense, but contracted it to Spergen limestone. 
From the standpoint of priority the name Salem should 
be used for this formation, but the Committee on Geologic 
Names of the United States Geological Survey has seen fit to 
adopt Spergen, in consequence of which the latter name has 
been more widely used in the literature than Salem. In the 
present report the formation will be referred to as the Spergen 
or Salem limestone. 
221st Rep. Dept. Geol, and Nat. Res, Indiana, pp. 289-427. 

ae ours ip i988 AY ol. 9, p. 215 (1901); also Geol. Surv. Ohio, 4th Ser., Bull. 
Bours Geol a Vales an, eon eae 
© Prof. Paper, U. S. Geol. Surv. , No. 24, table opp. p. 90; also Mo. 


Bureau Geol. and Mines, Vol. 2, 2nd Ser., p. 110 
7 Prof. Paper, U.S. Geol. Surv., No. 36, p. 28, 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 15 





Distribution. The Spergen or Salem limestone has a very’ 
limited area of outcrop within the Princeton Quadrangle. It is: 
exposed along the Evansville branch of the Illinois Central: 
Railroad, about one and one-half miles northwest of the station: 
at Princeton, just north of fault No. 38. One of the best out- 
crops of the formation is west of the Farmersville road, opposite - 
the exposure along the railroad just mentioned, in the side of 
the private road, only a few rods from the public highway. 
The entire area of outcrop of the formation at this place is small, 
being only a fraction of a square mile, with but few actual 
exposures, although it can be recognized over most of the area 
from the scattered residual material. 

Zathologic character. Although the Spergen or Salem beds: 
have been completely silicified in all surface exposures observed, 
they have not been changed to a true chert. All of the original 
structures of the limestone, the bedding, the organic remains, 
ete., have been retained. The silicified rock is very porous, and 
in the weathered portion, at least, it is a light, reddish-brown 
color. The rock is composed almost exclusively of fragments of 
fossils, but any complete specimens are rare. 

Thickness. The full thickness of the Spergen or Salem has: 
nowhere been observed in the area under consideration. There 
is room for a maximum exposure of about 40 or 50 feet beneath 
the St. Louis limestone, in the area where the formation is 
present at the surface in the Princeton Quadrangle, but it is 
not possible to determine how much deeper it extends. In the 
deep well at Cedar Hill the Spergen or Salem is undoubtedly 
present, but it has not been possible to recognize it as such or 
to distinguish it from the underlying or overlying members 
of the Series of formations, so there is no check on its thickness. 
at that point. In the Mississippi Valley south from St. Louis 
the thickness of the formation does not vary greatly from 160 
feet, although it is much thinner than this in southern Iowa,,. 
and also in the Indiana region where it was originally desecribed- 
The formation has not been well differentiated from the under- 
lying Warsaw in Hardin County, Illinois, but a limestone 
stratum of about 60 feet may be the equivalent of the forma- 
tion.8 In sections elsewhere, especially in the Mississippi Val- 


ee 


STll. State Geol. Surv., Bull. 41, p. 100 (1921). 





16 PRINCETON QUADRANGLE 





ley and in Indiana, a considerable portion of the Spergen or 
Salem formation is more or less oolitic in texture, but this char- 
acteristic has not been observed near Princeton. 

Stratigraphic relations. There is no evidence of any strati- 
graphic break within the Iowa Series of the Mississippian in 
this portion of Kentucky. Sedimentation seems to have con- 
tinued without interruption throughout the entire epoch, which 
eondition accounts for the absence of uneonformities between 
the several formational units, and also constitutes-one of the 
reasons why it is so difficult to draw any lines of sharp demarka- 
tion between the formations. 

Paleontology. The outerops of the Spergen or Salem, and 
also the residual material, are composed largely of organic 
remains, but good fossils are not common. As yet no thorough 
search has been made for a representative fauna, but a fairly 
good example of Melonechinus sp. and one of Dizygocrinus sp. 
have been picked up among the residual fragments of the 
formation. 

Correlation. The correlation of the beds referred to the 
Spergen or Salem limestone in the Princeton Quadrangle is 
based largely upon their stratigraphic position beneath St.. 
Louis limestone. The erinoid Dizygocrinus sp. closely resembles 
species described as coming from the St. Louis lhmestone in 
Washington County, Indiana, but at the time it was defined, 
the Spergen beds were commonly included with the St. Louis, 
and the type specimen undoubtedly came from true Spergen 
or Salem; no closely related species is known from beds that 
are truly St. Louis. JMZelonechinus also is more commonly met 
with in the higher portion of the Spergen than in the St. Louis 


proper. y 


Sr. Louis LIMESTONE 


Name. The St. Louis limestone was originally named from 
the city of St. Louis, Missouri, where the formation is finely 
developed. It has a wide distribution in the Mississippi and 
Ohio Valleys. 

Distribution. In the Princeton Quadrangle the St. Louis 
limestone is limited in its distribution to the Crider, Princeton, 
McGowan and Saratoga rectangles, in four distinet fault blocks, 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 17 





all of which are in the region lying to the southwest of the 
much faulted northwest-southeast belt which crosses the quad- 
rangle. There are two quite distinct areas of outcrop of the 
formation. The northernmost of these is an east-west belt about 
eight and one-half miles in length, varying from one to two 
miles wide, extending westward from the much faulted belt 
to the western edge of the quadrangle where the belt has its 
greatest width. The south edge of this belt is about one mile 
north of the center of the town of Princeton. This belt is 
divided diagonally, about three miles from its eastern extremity, 
by one of the longer faults of the region. The northern bound- 
ary of this belt is continuous, but its southern boundary is 
interrupted at the position of the diagonal fault by a small, 
wedge-shaped, down-dropped block of Pottsville sandstone. 
The southernmost of the two St. Louis areas occurs in two 
large fault blocks, and has been exposed by reason of the erosion 
of the overlying Ste. Genevieve limestone by Eddy Creek and 
some of its tributaries, the most important of which is Dry 
Creek. The boundary of the formation in this area is exceed- 
ingly sinuous except along the south side of the Otter Creek 
fault (fault No. 88), where the St. Louis limestone is continuous 
for over eight miles from the western border of the quadrangle. 
Tathologic characters. Good exposures of the St. Louis 
limestone are not common in the Princeton Quadrangle. Most of 
the area underlain by the formation is deeply covered with 
residual beds of red clay in which a great amount of chert is 
included. These residual clays are a conspicuous feature in the 
public roads, along the streams, and in gullies. The cherts are 
very little or not at al! more abundant in the St. Louis lime- 
stone areas than in some portions of the region underlain by 
the Ste. Genevieve limestone, but the St. Louis cherts are some- 
what different in character, and specimens of the fossil coral 
TInthostrotion are rather commonly met with in them. Much 
of the St. Louis chert is more dense and compact in texture, 
and less easily affected by weathering than a great deal of that 
in the Ste. Genevieve limestone, and many masses of it occur 
in more or less irregular chunks. No oolitic structure has been 
noticed in any of the cherts which are certainly of St. Louis 
age. Although there are distinct lithologiec differences between 


18 PRINCETON QUADRANGLE 





the cherts of the two formations, in many places it is not possi- 
ble to differentiate with certainty the St. Louis from the Ste. 
Genevieve by means of the cherts alone. 

The limestone exposures of St. Louis age which have been 
met with exhibit some variations in character. There are 
several exposures in the eastern one-third of the fault block in 
the Princeton rectangle bounded by faults 44, 45, 39, and 33, 
along Flynn Creek and its main tributary in this region from 
the west. In these outcrops the limestone is gray in color, more 
or less dense and compact in texture, and some of it includes 
much chert. These outcrops are all in the higher portion of 
the formation. An outcrop of the lower beds is present in the 
southwestern part of the same fault block, a little less than a 
quarter of a mile north of fault No. 39, in the valley draining 
into the eastern end of the large crescent-shaped sink hole just 
northwest of the corporation limits of Princeton. The limestone 
is Impure and dark in color, being interbedded with chert 
layers. The difference between the lower and higher beds of the 
formation is similar to that recognized in Hardin County, 
Illinois,? where the lower portion is made up of nearly black, 
impure limestone, the higher beds being much lighter and com- 
monly gray in color. 

More numerous outcrops of the formation are present in 
the southwestern portion of the quadrangle, more especially in ° 
the Saratoga rectangle, but even here the formation is largely 
covered with residuum. The limestone is gray to black in 
color in most places, compact to dense in texture, but in a few 
localities an oolitic bed has been observed in the lower portion 
of the formation as it is exposed. The cherts of the formation 
vary considerably at different horizons. In one zone near or 
below the middle of the formation there are numerous smooth, 
lenticular chert concretions with evenly convex sides and rather 
sharp periphery. These concretions vary in size from two or 
three inches to nearly a foot in diameter, and in places they 
occur in considerable numbers along stream channels in which 
this particular bed is exposed. Other chert masses are more 
or less irregular in shape. The more spherical chert concretions 
which are met with in the region are commonly from the lower 


* Tll;State.Geols Survy, cbull. wNoOs 41) tpeeee (19213 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 19 





portion of the Ste. Genevieve limestone, although similar cherts 
are rarely present in the St. Louis limestone in places. As in 
the formation north and northwest of Princeton, silicified speci- 
mens of Lithostrotion proliferum and L. canadense are met with 
commonly in the residual deposits. 


Thickness. None of the exposures of the St. Louis lime- 
stone in the Princeton Quadrangle are of such a character that 
the full thickness of the formation can be measured. In the 
southwestern corner of the quadrangle at least 200 feet of strata 
referable to the formation have been uncovered by erosion in 
some of the tributaries of Eddy Creek. The whole of the for- 
mation has been penetrated in the deep well at Cedar Hill, but 
its exact limits cannot be determined, either above or below. 
There certainly is as much as 300 feet of strata in the well 
section which must be St. Louis limestone, and probably con- 
siderably more, perhaps more than 400 feet. 


Stratigraphic relations. The stratigraphic relations of the 
St. Louis limestone in the Princeton Quadrangle are similar to 
those in other parts of the Ohio Valley. Sedimentation was 
continuous from the underlying Spergen or Salem, and _ also 
continued into the overlying Ste. Genevieve, with no strati- 
graphic breaks, consequently the formation is not set off by 
unconformities either below or above. Farther west, along the 
eastern flank of the Ozark region in southeastern Missouri, there 
is a distinct erosion unconformity between the St. Louis and 
the overlying Ste. Genevieve limestone, but the base of the for- 
mation passes by gradual transition into the underlying Sper- 
gen or Salem with no break. The unconformity at the top of 
the St. Louis in the region east of Ozarkia is undoubtedly due 
to one of the periodic uplifts of the Ozark dome which seems 
to have been raised repeatedly during the progress of Paleozoic 
time. : 

Ulrich has insisted that the boundary between the Ste. 
Genevieve and St. Louis limestones marks the lower limit of the 
Chester Series, and apparently infers that an important uncon- 
formity is generally present at this horizon. He has recognized 
the unconformity in Ste. Genevieve County, Missouri, and has 
attempted to show that in southeastern Tennessee the St. Louis 


20 PRINCETON QUADRANGLE 


limestone is in unconformable contact with both the Ste. Gene- 
vieve and the Spergen or Salem, and from these observations 
he has assumed that the St. Louis-Ste. Genevieve contact is 
unconformable across the entire intermediate area from the 
Appalachians to Ozarkia. He has published a photograph and 
sketch 1° of an exposure in an unused railroad cut five and one- 
half miles east of Jasper, Tennessee, in which he interprets 
certain partings in the rocks as the upper and lower boundaries 
of the St. Louis limestone, which he states is in uneonformable 
eontact both with the underlying Spergen and the overlying 
Ste. Genevieve, the greatest thickness of the bed considered as 
St. Louis limestone being less than ten feet. His only basis for 
identifying the so-called St. Louis limestone as such is the dif- 
ference in lithologic character, which is not important, and the 
belief that the partings which he has observed are planes of 
unconformity. No paleontological evidence is presented, and 
none could be presented, to show that the strata so designated 
are Spergen, St. Louis and Ste. Genevieve. 


In a recent examination by the writer of a series of sections 
including this stratigraphic interval in the Cumberland esearp- 
ment across Tennessee, it was found that the base of the Ste. 
Genevieve limestone is marked by a very persistent oolitie lime- 
stone bed which is especially characterized by numerous 
examples of the brachiopod Rhipidomella dubia. In most of 
the sections studied the St. Louis age of the strata beneath the 
Rhipidomella bed could be established by the presence of 
examples of the coral Lithostrotion canadensis or L. proliferum. 
At the Rhipidomella dubia horizon, or within a few feet of it 
the oolitie texture, so characteristic of the Ste. Genevieve lime- 
stone, is introduced, and the St. Louis limestone corals do not 
oceur above this horizon. The persistence of this bed, three or 
four feet in thickness, with its characteristic fossils, makes it. 
a most valuable key horizon, and if it is not the base of the 
Ste. Genevieve limestone it is close to that position. In the 
railroad cut east of Jasper, where Ulrich’s photograph and 
sketch were taken, this characteristic Rhipidomella bed is well 
exhibited 50 feet beneath the layer which he has designated as 


10Ky. Geoly Surv., Miss. Horm. West. Ky., plates’ H-l and Ei-23yepp. 
101-102 (1917). 





21 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 





‘UOTSdI 94} JO AYdeIsOdo}] UBIACAISSISSIP OLJSt1aJOBVIVYD ‘ssuTIdG 1B oy} Ysulvse pesypnvrys 
ST 9U0OJSIWIT BUUITA 94} JUSII SUlata}x9 94} JY ‘Ssuludg IBZ oY} Jo AaqmMeW JUOISpUBS T[BSeq 9} 
yyeoueq ssed uollewu0y UvBIq Us[yH 9Y} JO Speq A[VYS 9} Wal ey} FV ‘“Sainqs}}009 Jo 4sva ‘pvol 
-[ley [B1}JUa) SIOUTTII “IND S,9yoTVBAA UL UMOYS ATjUusT[eoxX9 SI 9sUuOJSpUBvS SSulIdS AB], IAISSBVUI OU, 
TOO SAHOIVM HAO VNVYUONVd 





22 PRINCETON QUADRANGLE 





the sole representative of the St. Louis. The upper part of the 
true St. Louis limestone is present in the section, being repre- 
sented by beds of very cherty, compact limestone, similar in 
all respects to the St. Louis elsewhere in Tennessee, and there 
is no reason to believe that the formation is represented by any 
less thickness of strata here than elsewhere in the state. The 
so-called St. Louis of Ulrich is simply a local bed in the Ste. 
Genevieve, more cherty than the beds above and below it, and 
the stratigraphic value of the partings bounding the bed are 
vastly overestimated by him. 

Paleontology. Good fossils are not numerous in the St. 
Louis limestone of the Princeton Quadrangle. Among the chert 
fragments along the road sides, in stream beds, and in gullies, 
silicified examples of the two species of the coral genus Lithos- 
trotion are not infrequently met with. Less frequently some 
other fossils, for the most part imperfect brachiopods, are seen, 
but the fauna as a whole is rather meager, and no attempt has 
been made to make complete collections. 

Correlation. The presence of the species of Lithostrotion, 
mentioned above, is sufficient to establish the correlation of the 
St. Louis limestone in the Princeton Quadrangle with this wide- 
spread formation of the Ohio and Mississippi Valleys, these 
corals being known from no other horizon. 


Srre. GENEVIEVE LIMESTONE 


Name. The Ste. Genevieve limestone was first named many 
years ago from the exposures in the vicinity of Ste. Genevieve, 
Missouri. Ulrich first described the formation in Kentucky as 
the Princeton lmestone,!! but later he recognized that his for- 
~mation was equivalent to the Ste. Genevieve and consequently 
adopted the older name first apphed by Shumard in 1859 from 
exposures at Ste. Genevieve, Missouri. } 

Distribution. In the Princeton Quadrangle the Ste. Gen- 
evieve limestone underlies a larger proportion of the surface 
than any other single formation, but its entire distribution lies 
southwest of the conspicuous northwest-southeast belt of fault- 
ing. A number of smaller fault blocks in the northern portion 


grey eaecae cat Préss, Dec., 1890;- Bull. U..S. Geol, .Surv., Nol2it= pecs 
( F 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 23 





of the Princeton rectangle are made up wholly or in part of 
Ste. Genevieve limestone. Two larger fault blocks in the Crider 
and Flat Rock reetangles include much more extensive areas 
of the formation, but all of these are separated from the most 
extensive area of the Ste. Genevieve limestone in the quadrangle, 
by the east-west belt of St. Louis limestone north of Princeton 
which has already been described. This larger area of the for- 
mation extends southward and westward from Princeton to the 
borders of the quadrangie, and is continuous in these directions 
except where erosion has cut through this limestone into the 
St. Louis in the southwestern portion of the area. This large 
area is crossed by three east-west faults between Princeton and 
the southern boundary of the quadrangle, which produce a 
series of offsets in the contacts between the Ste. Genevieve and 
the underlying and overlying formations. Along the southern 
boundary of the quadrangle the total length of outcrop of the 
Ste. Genevieve is over ten miles. 


Topographic Hxpression. Within the area occupied by the 
Ste. Genevieve limestone the land surface is characterized by 
gentle slopes, and a large portion of the area is tillable farming 
land. The area is particularly characterized by imnumerable 
sink holes, varying in size from a few feet to as much as a mile 
in maximum dimension. These sinks dot the entire area, and 
through them the drainage is mostly underground, so that only 
a few valleys occupied by major streams or tributaries are 
present. 

Subdivisions of the Ste. Genevieve. In Ulrich’s !? redefini- 
tion of the Ste. Genevieve limestone, he recognized three mem- 
bers, the Fredonia oolite below, followed by the Rosiclare sand- 
stone, and the Ohara limestone at the top. In the original defini- 
tion of the Ohara, the type locality being at Cedar Hill quarry, 
formerly known as Ohara Post Office, the Renault lmestone 
was included as part of the member. Later studies have proven 
that only the lower part of the original Ohara is of Ste. Gen- 
evieve age, so that the subdivisions recognized in this report 
are I'redonia oolite, Rosiclare sandstone, and Lower Ohara lime- 
stone. No Upper Ohara limestone is recognized as such in the 


Wes. Geol, oUurve, rot, Paper No, 36, p. 39.G905). 


24 PRINCETON QUADRANGLE 





section, however, for those beds constitute the Renault limestone 
at the base of the Chester Series in the general section. By 
far the greater portion of the formation is included in the 
Fredonia member. 


Lithologic characters. Some portions of the Ste. Genevieve 
limestone are not essentially different in lithologie character 
from some of the higher beds of the St. Louis limestone. Both 
formations are cherty, and great quantities of fragmentary chert 
in red clay are present in the residual accumulations from the 
limestones. There is some difference in character between the 
cherts from the two formations, but the differences are not suf- 
ficiently marked to make it possible in all cases to differentiate 
the formations from the cherts alone. One of the most char- 
acteristic lithological features of the Ste. Genevieve limestone, 
is the presence of beds of oolite. Only rarely has oolitie lime- 
stone been observed in the St. Louis, and in practice the field 
eeologist draws his boundary line between the two formations 
below the last bed of oolite. The Ste. Genevieve limestone, how- 
ever, is not oolitic throughout, and many beds, especially in the 
lower portion, are indistinguishable by themselves, from the 
St. Louis limestone. The oolitic beds become more and more con- 
Sspicuous in passing upward in the formation, and the upper 
half of the Fredonia member is largely oolitiec in character. On 
the whole the Ste. Genevieve is a whiter limestone than the 
St. Louis, the oolite beds especially being white in color. The 
oolitic texture is recognizable in some of the cherts of the Ste. 
Genevieve, this being one manner in which some of the Ste. 
Genevieve chert can be distinguished from that of the St. Louis 
limestone. In some portions of the formation the chert con- 
eretions are more or less globose in form, with smooth surfaces, 
such masses ranging up to ten inches or more in diameter. 
Similar, smooth, rounded cherts do occur in places in the St. 
Louis, but they are more common in the Ste. Genevieve, much 
of the St. Louis chert occurring as rather rough, more or less 
irregular masses. The higher, more oolitic beds of the forma- 
tion are less cherty than the lower portion, some residual clays 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 25 


from the higher Fredonia being deep red in color and quite 
free from chert, but elsewhere the chert is present to the top 
of the Fredonia at least. 

The Rosiclare sandstone member of the Ste. Genevieve is 
reddish-brown or yellowish-brown in color as it 1s commonly 
exhibited in its weathered condition, being fine grained and 
porous in character. Where it occurs in an unweathered con- 
dition, as shown in the Cedar Hill quarry, it is gray or greenish 
in color, and is more or less calcareous. In its original condi- 
tion it is probable that the bed was everywhere a calcareous 
sandstone or arenaceous limestone, and that it only appears as 
a porous sandstone on the weathered outcrop. The Rosiclare 
varies from place to place in regard to its bedding, some por- 
tions of the sandstone being thinly bedded while other parts are 
more massive. 

The Lower Ohara member of the Ste. Genevieve limestone 
resembles-the Fredonia in its lithologic character. It includes 
oolitic Limestone beds along with others which are more or less 
erystalline. <A series of Lower Ohara beds out of connection 
with the Rosiclare sandstone or the overlying Renault lime- 
stone, would possess no lthologic character which would cer- 
tainly differentiate them from a similar series of beds in the 
Fredonia. 


Thickness. In the southernmost fault block in the Prinee- 
ton quadrangle, the entire width of outcrop of the Ste Genevieve 
limestone is present from the St. Louis limestone below to the 
Renault above, this width being a little over ten miles. In this 
same area the basal contact of the formation can be followed 
continuously for several miles, and a drop of 80 feet in four 
miles can be observed. This would give, with a uniform dip, a 
total drop of 200 feet for the basal contact in the entire width 
of outerop. The elevation of the lower and upper contacts of 
the formation in this area are essentially the same, so that a 
thickness of 200 feet may be accepted as the minimum for the 
formation. The deep well at Cedar Hill gives some check on the 
thickness of the formation, for the first samples saved, at a 
depth of 250 to 255 feet are clearly in the St. Louis limestone, 
and by adding 70 feet, which is the interval between the eleva- 


26 PRINCETON QUADRANGLE 














tion at the mouth of the well and the summit of the formation 
in the Cedar Hill quarry, a maximum limit of 320 feet is estab- 
lished. How much less than this the actual thickness of the 
formation really is, has not been determined. Observations in 
Hardin County, Illinois, have led to an estimate of 3800 feet 
as the maximum thickness of the Ste. Genevieve, and a similar 
thickness may perhaps be expected about Princeton. 

Of the entire thickness of the Ste. Genevieve limestone the 
Fredonia constitutes much the larger part. The Rosiclare sand- 
stone member is thin, varying from two feet to twenty. The 
Lower Ohara varies somewhat because of the erosion interval 
which succeeded it, its maximum thickness being perhaps 50 
feet. 

Stratigraphic relations. The Ste. Genevieve limestone 
rests with entire conformity upon the St. Louis. Because of 
the deep covering of residual materials, composed of quantities 
of chert imbedded in red clay, the actual contact of the two for- 
mations has nowhere been observed in the Princeton quad- 
rangle, and the mapping of this boundary is most difficult. No- 
where in the section is there any sharp demarkation of the two 
formations, but in general the St. Louis is made up of more 
dense and compact limestone beds, although there are just as 
dense and compact beds in the Ste. Genevieve as any of those 
in the St. Louis. In the Ste. Genevieve limestone oolitic lime- 
stone beds are commonly present, but not all of the formation 
is of. that character, and in a few localities oolitic beds have 
been observed in undoubted St. Louis limestone. The St. Louis- 
Ste. Genevieve limestone represents one continuous geologic 
epoch during which the conditions of sedimentation were grad- 
ually changing, and the lower St. Louis limestone in western 
Kentucky is distinctly different from the upper Ste. Genevieve. 
The upper St. Louis, however, and the lower Ste. Genevieve are. 
much ialike and there are some 40 to 50 feet of Lmestones which 
might be placed in either formation so far as the. Jlithologic: 
characters are concerned. ‘agt ia eae 3 

-The fossils furnish some assistance in ‘separating the two 
formations, although in neither of them are the fossils.:either: 
abundant : or -welld preserved: except very locally. : "Fle :doral. 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 27 





genus Lithostrotion, represented by two species, L. proliferum 
and lL. canadense, is one of the most common fossils of the St. 
Louis limestone, and neither of these species have been observed 
in the Ste. Genevieve limestone. These corals are commonly 
silicified and occur in many places with the residual cherts, and 








Jiuds 3-- TPPpER PORTION TAR SPRINGS SANDSTONE. 
»-*Shale and impure coal bed: in’ Tar Springs Sandstone, Walche’s Cut, 
Illinois Central Railroad, east of Scottsburg. 


28 PRINCETON QUADRANGLE 


their presence in such situations has been taken as evidence of 
the presence of the St. Louis limestone. 

The fossil form which is the best indicator for the Ste. 
Genevieve limestone is the crinoid Platycrinus penicillus. This 
species 1s represented most commonly by the separate stem 
segments which have the elliptical form characteristic of the 
genus, and are ornamented by a series of projecting spines about 
the margin. The bases of the crinoid are also common in places, 
and may be easily recognized by the three ridges radiating from 
the stem facet. This crinoid is not restricted to the Ste. Gen- 
evieve, being also present in the St. Louis, but it is much more 
abundant in the higher formation. 


In field practice, where the limestone outcrops are scarce 
or wanting, careful search has been made for loose specimens 
of silicified Lithostrotion in gullies and along roads, and the 
highest occurrence of such specimens is assumed to be some- 
what below the contact between the two formations. 


In general the red clay residuum of the Ste. Genevieve, 
especially the Fredonia limestone, is much deeper red than that 
of the St. Louis, and in the higher part of the formation, in many 
localities, it is quite free from chert. In the basal part of the 
Fredonia, however, overlying the last of the Lithostrotion bear- 
ing cherts, there is a characteristic, highly cherty residuum with 
deep red Fredonia color, and including great numbers of smooth, 
sub-globular cherts varying from two or three inches to ten 
or twelve inches in diameter. In the absence of limestone out- 
crops this type of residuum has been mapped as basal Ste. Gen- 
evieve limestone, for it distinctly overlies the Lithostrotion bear- 
ing beds. Somewhat similar globular cherts do oceur in places 
in the St. Louis limestone, but never in such abundance. 


At its upper boundary the Ste. Genevieve is succeeded by 
the Renault limestone, from which it is separated by a distinet 
unconformity, which will be discussed in connection with the 
description of the higher formation. 


Paleontology. Fragmentary remains of fossils are every- 
where present in the Ste. Genevieve limestone, but well pre- 
served fossils are not commonly met with. The best fossil mate- 
rial has been collected from certain shaly beds near the top 


STRATIGRAPHIC GEOLOGY—IOWA SERIES 29 





of the Fredonia member. <A very characteristic feature of the 
weathered surfaces of this Ste. Genevieve limestone is the pres- 
ence of the elliptical stem plates of the ecrinoid Platycrinus 
penicillus, with their characteristic marginal spines. Upon some 
beds these Platycrinus plates are wanting, but if any consider- 
able exposure is available, they ean be found in almost any 
locality. The same sort of plates are also present, but less 
commonly, in the St. Louis limestone, but wherever such plates 
are really abundant the limestone is quite certainly Ste. Gen- 
evieve. The plates are present in both the Fredonia and Lower 
Ohara members of the formation. They have nowhere been ob- 
served above the Ste. Genevieve. 


Locally in the upper part of the Fredonia member, there 
are numerous masses of a colonial coral, Iithostrotion har- 
modites, which is known in no other formation. The coral masses 
attain dimensions of a foot or more across, and have been 
observed very commonly along the public road running north- 
east from Bethlehem School, one mile north of Crider. 


A characteristic Ste. Genevieve limestone fauna, from the 
upper part of the Fredonia member, one mile northeast of 
Crider, contains the following species: 


Lithostrotion harmodites (M.-E. & H.) 
Michelinia subramosa Ulrich. 
Unidentified coral. 

Pentremites princetonensis Ulrich. 
P. pulchellus Ulrich. 

Platycrinus penicillus M. & W. 
Bryozoan. 

Productus sp. cf. P. parvus. 
Pustula genevievensis (Weller). 
Rhipidomella dubia (Hall). 
Pugnoides ottumwa (White). 
Girtyella indianensis (Girty). 
Spiriferina sp. 

Spirifer pellaensis Weller. 
Reticularia setigera (Hall). 
Humetria verneuilana (Hall). 
Cliothyridina sublamellosa (Hall.) 
Composita trinuclea (Hall). 
Aviculopecten sp. 

Platyceras sp. 


30 PRINCETON QUADRANGLE 


A fauna from a similar horizon, .8 mile north of the last 
mentioned locality and one and one-half miles northeast of 
Crider, has furnished the following species: 


Lithostrotion harmodites (M.-E. & H.) 

Cystelasma sp.? 

Platycrinus penicillus M. & W. 

Dizygocrinus persculptus Ulrich. 

Pentremites princetonensis Ulrich. 

P. pulehellus Ulrich. 

Productus ovoides (Hall). 

Productus sp. 

Rhipidomella dubia (Hall). 

Girtyella indianensis (Girty). 
ugnoides cttumwa (White). 

Spiriferina sp. 

Spirifer sp. 

ELumetria verneuiliana (Hall). 

Cliothyridina sublamellosa (Hall). 

Composita trinuclea (Hall). 

Platyceras sp. 


CHAPTER IV. 
STRATIGRAPHIC GEOLOGY, CHESTER SERIES 


Every one of the formational units which have been recog- 
nized and described in the Chester Series of the Ohio Valley 
has been identified in the Princeton Quadrangle. The best: 
locality for the exhibition of the entire succession of Chester 
formations is in Walche’s cut on the new line of the Illinois 
Central railroad a little less than two miles northeast of Scotts- 
burg. A number of faults cross the cut so that portions of some 
of the formations are not exposed by reason of the dislocation 
of beds which has taken place, but every one of, the Chester 
formations except those above the Palestine sandstone is exposed 
to some extent, and the higher formations are present in the cuts 
between the end of Walche’s cut and Claxton station. The 
older formations of the series are exhibited in the western part 
of the cut, the younger ones to the east. No excavation could 
have been made anywhere within the Quadrangle to exhibit the 
Chester succession more completely than is done in this rail- 
road cut. 


RENAULT LIMESTONE 


Name. The lowest formation of the Chester Series in the 
Ohio Valley is the Renault. In the Mississippi River section the 
Aux Vases sandstone separates the Renault from the underlying 
Ste. Genevieve limestone, but this sandstone is represented by 
a part at least of the time interval of the unconformity between 
the Ste. Genevieve and the Renault. In the Princeton Quad- 
rangle and throughout the Ohio Valley the Renault is for the 
most part limestone with some shale partings, but in the Missis- 
sippl Valley, where the formation was first named from Renault 
Township, Monroe County, Illinois, it contains sandstone mem- 
bers and also some extensive shale members. 

Distribution. The distribution of the Renault limestone in 
the Princeton Quadrangle is along a belt from four to five miles 
or less in width, extending from the southeastern corner of the 
quadrangle to the, western border about three miles from the 
northwestern corner. The actual outcrop of the formation - 
within this belt is ‘rarely more than'a fraction ‘of.'a\ mile in. 


32 PRINCETON QUADRANGLE 








width. The outerop is extremely sinuous and irregular in its 
distribution within the broader belt mentioned, and lacks con- 
tinuity because of the fault dislocations within the belt. 
Throughout much of its extent the Renault outcrop occupies 
rather steeply sloping hillsides, which are capped by the Bethel 
sandstone, and at whose base the Ste. Genevieve limestone 
spreads away in a comparatively level surface. The distribution 
of the formation in detail is shown upon the accompanying map. 


Iithologic characters. The Renault limestone is somewhat 
variable in character, although it is rather persistently gray in 
color, some parts of it being nearly white, and some yellow 
or buff beds are locally present. The weathered surfaces are 
commonly smooth and rounded where they are well exposed. 
The texture varies from dense and compact to more or less 
erystalline, the yellow beds, where present, being somewhat 
earthy. Most of the beds are hard, breaking with a more or 
less splintery fracture. The limestone layers are commonly 
separated by shaly partings, and at some horizons, especially 
towards the top of the formation, there are beds of caleareous 
Shales two or three feet thick in places. The basal, more shaly 
beds which are so well developed in the Goleonda Quadrangle 
in Livingston County, and the adjacent Hardin County, Illinois, 
and which have been called the Shelterville member of the for- 
mation,! are not well exhibited in the Princeton Quadrangle. 
Hither this part of the formation is not present in the area, or 
as is more likely, it is represented by some of the limestone 
beds. 

At the base of the Renault, just above its contact with the 
underlying Ste. Genevieve limestone, there is very persistently 
present a conglomerate or brecciated layer about one foot, more 
or less, in thickness. This layer has been observed in numerous 
localities in the quadrangle, and doubtless it is present through- 
out the area. In those places where the bed has not been 
observed it probably is present, but is now covered with super- 
ficial material. The fragments included in this conglomerate 
or breccia are all limestone, and are commonly somewhat dif- 
ferent in color and somewhat more dense than the gray matrix in 


1711, State Geol, Surv., Bull. No. 41, p. 1838; also Jour. Geol., Vol. 
XXVIII, p. 290 (1920), 











DETAIL OF RENAULT LIMESTONE. 


These beds occupy a nearly horizontal position in Walche’s Cut, Ill- 
inois Central Railroad east of Scottsburg. 


which they are inclosed. They are angular to rounded in out- 
line and vary in size from a small fraction of an inch to an inch 
or more across. This layer is undoubtedly associated with the 
unconformity which exists between the Renault and the under- 
lying Ste. Genevieve limestone. — 

Thickness. The Renault formation varies somewhat in 
thickness within the quadrangle, although this variation is not 


at “PRINCETON QUADRANGLE 








excessive. Its usual thickness is about 80 feet, but in a few 
places it seems to be less than this, perhaps as little as 60 feet, 
and elsewhere it seems to exceed the average thickness, and may 
be nearly 100 feet thick. 3 


Stratigraphic relations. The unconformity at the base of 
the Renault is the most important stratigraphic break in the 
whole Mississippian System in the Ohio and Mississippi Valleys, 
being the boundary line between the Iowa and Chester Series. 
The withdrawal of the sea from the interior of the continent was 
more complete at this time than at any other, and with the 
readvance of the sea into the Chester embayment, the new faunas 
of the Chester Series were introduced. Aside from the notable 
faunal change in passing from the Ste. Genevieve into the 
Renault limestone, the presence of the conglomerate or breccia 
‘bed at the base of the Renault is good physical evidence of the 
unconformity, and where the actual contact between the two 
formations can be seen there are some irregularities in the sur- 
face upon which the younger sediments were laid down. 

The contact between the Renault and the overlying Bethel 
sandstone has nowhere been observed in the Princeton Quad- 
rangle. There is an abrupt change, however, from the lime- 
stone to the sandstone, and where the contact has been seen in 
Hardin County, Iilinois,? there is no doubt of an uneconformable 
relation, and the same condition doubtless exists throughout this 
portion of Kentucky. 

Paleontology. The Renault limestone is characteristically 
the zone of the ecrinoid genus Talarocrinus. A number of dif- 
ferent species of the genus have been described from the faunas 
of this formation in Kentucky and southern Illinois, but the 
genus is entirely unknown in the Ste. Genevieve limestone 
faunas, and it is rare in the next higher limestone formation, 
the Paint Creek, being unknown from any other horizon in the 
Chester Series. This Talarocrinus faunal zone is a most char- 
acteristic feature of the Renault limestone from Monroe County, 
Illinois, across the whole of southern Illinois, into Kentucky. 
Among the other forms associated with Talarocrinus may be 
mentioned the bryozoan Cystodictya labiosa. The genus Cysto- 


—_—_ 


2Tll. State Geol. Surv., Bull. No. 41, pp. 146-147. 





STRATIGRAPHIC GEOLOGY—CHESTER SERIES 35 





dictya has not been observed in any Ste. Genevieve lhmestone 
fauna. The species C. /abiosa occurs in many localities in the 
Renault, but it does not become really abundant until the Paint 
Creek. Higher than the Paint Creek neither the species nor 
the genus are known, so that in association with other things 
this bryozoan is useful in some places in determining the horizon. 
Another feature of the Renault fauna is the presence for the first 
time of the pyriform species of Pentremites. A few species 
pass over from the. Ste. Genevieve into the Renault, but all of 
them are long range types that are either present or are repre- 
sented by closely allied species in faunas still older than the 
Ste. Genevieve. The most characteristic elements in the Renault 
faunas are the characteristically Chester forms which are intro- 
duced for the first time. The most prolific fauna of the Renault 
in western Kentucky is that of the basal, Shetlerville member 
of the formation, which is not well developed in the Princeton 
Quadrangle. The hard limestone beds of the formation are not 
of a character to permit the preservation of the fossils in good 
eondition for collecting, but there are some shaly beds which 
have furnished small but very characteristic faunas. 

At the Cedar Hill quarry fossils have been collected from 
three different beds in the Renault limestone, one near the base, 
second from a shale bed near the middle, and third from a lime- 
stone bed at the top of the formation. In the following list all 
of the species which have been recognized from the three beds 
are recorded, their occurrence in the three different beds being 
indicated in the three columns, 1, 2, and 3, numbered from the 
lower to the higher. 


Renault Faunas from Cedar Hill Quarry 











| nh | 2 3 
Triplophyllum spinulosum (M.-E. & H.) ...22--2--..-.... | | : ? 
ECOGTLNUS 8 DILL SEO AIITIGU 5,0 cjsecanct ston se detes cat eee aetna - a a 
PRIEEOC TI IIL SLT LT LOLS aN ue,” Ure esas co aasdnst-nnccede sence seus | | ied - 
ert Ceirties. COCONT DOP TANCE) cacktscse-.incveronebeeenece cers | * ee 
Pentremites duttsi Ulrich .....c.c.ccccececcesesesseeseseeeeeeeeeee | xe | ** 
EATEN EMSS BY ODg gis ie aes, 2 ani re, Oe fear aaa a a a * ae 
SPEIER EAVES SLL ee, ores ee tcc ec no ee vn Poms is aove te case ope cate | * 
Fistulipora excelens AOD Cle eye tec pros ae coat), Oa eR eee | * * 


36 PRINCETON QUADRANGLE 


Renault Faunas from Cedar Hill Quarry—Continued. 








ETL ODONG:. SP. < cea eee eect sere ie eee | 
DaLOSLOMELA SHINUIOSG. GITIC, 222 ee ee | 
PENCSTCLIGALENGT AO L1G ere eee ee ee ee | 
Penesteula. SCT raat UATAG igs 2 eee ee 
DEUHECSTELIGSCESETICNSTS OU LDICL pine eee erie eae 
SP OLYUDOTE  COSETICTISTS MULITACIY ce erica eee ee ee 
POLYOL: SD tapes 5 ores ete or ee ne ee 
HSV ODOT S CUANCUNCLOIS SULT IC hee ee | 
TUT ODOEGHS Dap ee ee ee ae ee ee me | 
SEDLODOTGLSUDO WOOT UIUS ULL GC Dae rene eee eee 
WYStOdiclrye “1d 01OSGa WW CllC time pee ces see ee eee 
MGLYDLONOTAADUNCELNOTE Wlrichwee =. ae te 
SPRLOCTODOTU: SDA oe er ee ee en 
Orthotetes kaskaskiensis (McChesney) ...............--- 
PrRODUCTUS JODAUIUS Sra) Bae cn A eee 
WrGaductus inflatis AicChesney 2222.2. 5.-c: oc seers eee 
WiGonragmus. elegans CN Gel)? o.oo eee 
Girtyella ind1anenses > ( GAPEy) Meee eee 
Girtyella brevilobatus (Swallow) ............----..---------- 
Spiriferina transversa. (McChesney )* _..... 20.2. 
SPIT1] CrING “SPUN SUN. Gy a) ree ee 
Spistfer pellaensis WW Cer jo ase cates ss eters ne sarees 
Spirifer increbescens var. transversa Hall ....- Peek 
SPAT ePer etd tens See mses eke eee ooo ere een ee 
Eagmnetria’ Vera. (Ea) ) 6 ierec cae tae reece oe nep ere ecar a 
Cleiothyridina sublamellosa (Hall) .......-.-..2--------- | 
Comnposita trinucted, -( Elall) Wi are ee ee 
Senizodus  SPr vive. ae earn eet cerca career | 
Orthonychia cf. chesterensis M. & W. ...-...--..----------- 
Euomphalus cf. planidorsatus M. & W. ......------------ 
PHAUIDSIONS Dc ee a pe ete ses 
CIATODUS? SD ee a a ee ee comet ee 





* | 





% * & & # 





Mice ane, oak Ss 


Cite ea: 








* i 


Very good collections have been made from the higher part 
of the Renault limestone at two localities northeast of Otter 
Pond, the first from about three-fourths of a mile from the rail- 
road station and the other about one and one-fourth miles from 
the same point. Both collections are from shaly beds, and it 
is not improbable that the horizon is the same at the two local- 
ities. A combined list of the species in these collections is given 
below, the two occurrences beine indicated in the. columns 


I and?2* 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 37 


Renault Faunas Northeast of Otter Pond 





ra PIODRUMUNEESDINWIOSIUNL. CM. Hiv 6c U TH. ) oi. .iessestaensce neces -ceeeee 
TOLEPOCTINUS, SD. 2:...!..-2.2- CR al TT oh RS 2 IER TB, od eB Sa | 
SerererreriaAtese atid. SLES. eee ee ee Be cu te ance eee save | 
PCILELEIMALES (DTINCELONCTISIS. UITICIY 8. lasetucncee 22.) ese eee 
Perteteie SDINES ay DIAUCS ten. neers masta ale ocsea Si cgosdnak abe ets 
PEPREILET UT Ge CCCLENSs WAP Chy oo sekec2c 5. Uist edeencacaesedededeilaacteemesmeaes Soe * 
RRR EERO T AEM TIOEIL CULIIOT UE Ul LEI CL pac tees ots eat oc onncesQtonssuneste-2n-caeiren-: 
228 Deh OW Teg ATG ODOC TAU fs AO ah CD AT ky em ee ae 
serMEML EGE LLORES) Sek ct ween OL cee oRUER., on cncadahegre écdectnstestecens 
PEEL PCNA ILO CT CULE Ce ae LOU Ly ieee oe sap iesc ons eaten eet ee ode enn 
2 ENGR CO TOA TO) ei tices SNe OR Sala os ee Se Ne es 
ee STC TICS SCUTTLE LU WOITIGIY 22020 catepcee bos one cteeh satoase settee end. oe 
ree eT (herd 7 OChGOR LT LGU. 221, tan ee oe sce bare ope ed nanan e~ -condeteceaeesei-oe 
TRS Veet WE Sea Mead | 27h, OURS OS OA en ee ee 
JEG SEE CHUB Eee SS oo 2 RL ES Reis mn ee Se 
PeereTEVOUOTU. CILUCT CINCO, WATICHS .. 2... nccc00se2-caednseeeedietewenecsuaes 
Ne OO UE LAE LD LOS (he W CLL OT cdncccascekedonaroccartnc-otagsbe atdegar tees <2lacate 
EE MES RR 3S eo OE Less | Pane wok 
Ori notceres Kashaskiensts (MCCHESNECY )  .2....c22..00.cnck--cecceceseee-s | 
RS TIA SGT GRR ol ws IST To Se Rae a ean Oe 
SER et IMGES CLE O (IESE IN GaGCU Ls). cesneresete sateen c aekeececeonees docs--te----=2 
AES GMA LULILOTSEIVS IS AW CLIGY occs.tn ten sadpay ss vlece centakceedaesovnke aetsasus 
ENSUE RAR OTRO THAR ELI NS ORs CC I) eee ota ave ROL Ey eee aoe Sense 
CCL ROE ULLOUULOD (Wall OW, ) lo rsenc- tes Sesswecibecse-c--s2 5 cesses scce 
spirierimasiransversa. (MeéChesney) .-02226)..--.: fetes eee 
Spirifer increbescens var. transversa Hall .........-.-.--....--000 
SUES BURR ECS OSS Ea Oe EN Seg ENS BNE oes 2 PRR ie oY ee ee 
TEE SVE AG R12 0 9 os Hs PT Ay ae na 
I OTILUVACTIE SUD CIIVELLOS (CRT ANT ) ic secre ace ede oe oa ee Sec ees 
rr nOetLG erence. (Hall) oe see a ee aeons ee ah 
EN Sa OPES Se gh eh Bec EP ih en et Rc Aap Nan: SOR a 
Lek SIN ESTATE GT SSE 6 BUD Ie Desay ERO tes By: OEM ORES WAP ie, 5 Se ee 
ENT 0 IRI TIES VI CBRL 4 ee elle Uhr Bp aes i ie nie or Dk de Ae A ar 
eter CLUVOLG. (NLCGUESIIOY ) ( caiicaltedsietc- db. Recaectdeneceseascsutes ¥ 
Cs 8d CACY Tey OND BE Ap Aaa eee Oe so 


* + & *& 
* %*%¢ + & 





* * * * * * * * * * * % % 
* 3 


re ee i A Ce RS at SS 
* 


+ + 


ss 
wr 


s + 





Se Ce ee Sci ei go SR 2c 








Along the lower slopes of the hillside one-fourth mile west 
of McGowan Station, some silicified Renault fossils occur in the 
red residual clays, and from this locality the following species 
have been identified : 


38 PRINCETON. QUADRANGLE 





Renault Fossils from Near McGowan 


Triplophyllum spinulosum (M.-E. & H.) 
Talarocrinus trijugis M. & G. 
Pentremites princetonensis Ulrich. 
Pentremites buttsi Ulrich. 

Spiriferinag sp. 

Cleiothyridina sublamellosa (Hall). 
Composita trinuclea (Hall). 


From some localities in the Renault limestone of the Prince- 
ton Quadrangle, a fauna somewhat different from those recorded 
above, has been collected. It is a fauna which seems to be 
associated with thin shaly partings between more massive lime- 
stone beds, which are really rather shaly limestone layers. From 
such a bed, one mile north of Princeton, the following species 


have been collected: 


Renault Fossils from North of Princeton 


Triplophyllum spinulosum (M.-E. & H.) 
Cystodictya labiosa Weller. 

Orthotetes kaskaskiensis (McChesney). 
Productus ovatus Hall. 

Diaphragmus elegans (N. & P.) 
Spiriferina transversa (McChesney). 
Spirifer breckenridgensis Weller. 
Spirifer cf. pellaensis Weller. 
Cliothyridina sublamellosa (Hall). 
Composita trinuclea (Hall). 
Platyceras sp. 


In this fauna the large brachiopods, Orthotetes kaskas- 
kiensis and Productus ovatus are by tar the most numerous 
species, the remaining forms being represented by a very limited 
number of individuals. 

Correlation. The question of the correlation of the Renault 
limestone has been fully discussed in the report on Hardin 
County, Ilinois,*? Ulrich included the formation in his Ohara 
member of the Ste. Genevieve limestone, and seemingly because 
of its Chester fauna he transferred the whole of his Ste. Gen- 
evieve limestone to the Chester Group. Extensive faunal studies 
of all of these beds, and the detailed mapping of the formations 


7Tll. State Geol: Surv., Bull. No. 41, pp. 150-159 (1921). 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 39 


entirely across southern Illinois and into western Kentucky, 
have established the fact that the inclusion of the Ste. Genevieve 
limestone proper in the Chester Series is entirely unwarranted. 
The detailed field studies continue to pile up the evidence for the 
exact correlation of the ‘‘ Upper Ohara’’ of Ulrich’s section with 
the Renault limestone of the Mississippi Valley section. The 
bed has now been actually traced and mapped in detail from 
Caldwell County, Kentucky, to and across Union County, 
Tllinois. 

it has been shown elsewhere that the Renault (‘‘Upper 
Ohara’’) limestone fauna, including that of the Shetlerville 
member, from Hardin County, Illinois, is essentially the fauna 
of the typical Renault of Monroe County, Illinois, with the 
exception of three species which have been described as new 
and which are known only from the Shetlerville. It has also 
been shown that the diagnostic fossils of the Ste. Genevieve 
limestone, Platycrinus penicillus and Pugnoides ottumwa are 
entirely unknown from the Renault (‘‘Upper Ohara’’) or any 
other Chester fauna. The species which are common to both 
the ‘‘Upper Ohara’’ and the Ste. Genevieve are in nearly every 
case long range forms which either are present in pre-Ste. 
Genevieve beds or are represented there by closely allied forms. 
The observations which have been made in Kentucky during the 
past two field seasons have confirmed the earlier conclusions in 
regard to the relationships of the faunas, in every respect. The 
correlation of the so-called ‘‘Upper Ohara’? with the typical 
Renault is established beyond question, and the extension of the 
name Renault into southern Illinois and Kentucky is fully 
justified. 


BETHEL SANDSTONE 


Name. In his description of the Mississippian section in 
western Kentucky, Ulrich* described a sandstone formation 
resting upon his Ohara member of the Ste. Genevieve limestone, 
which he identified as the Cypress sandstone of Engelmann, 
originally described from southern Illinois. In 1915 the writer 
established the fact that the Cypress of Ulrich was not the 
original Cypress of Engelmann, but a lower member of the 








Senormmapern Wah 2 Gel. sUinv., ANOM ob. p.roo (1905), 


40 PRINCETON QUADRANGLE 





Chester Series. A statement to this effect was made in Decem- 
ber, 1915,5 and the correction was accepted by Ulrich. In 1917 
Butts proposed the name Bethel sandstone ® for this formation 
which Ulrich had erroneously called Cypress, a name which 
has been adopted and used by all later workers in this field. 


Distribution. The distribution of the Bethel sandstone in 
the Princeton Quadrangle follows closely that of the underlying 
Renault limestone. The usual dip of all the strata throughout 
the area is to the northeast, and in general this sandstone under- 
hes a cuesta slope, much interrupted and broken by faults, 
sloping northwestwardly from the summit of the bluff-like 
exposures of the Renault. If the earth’s crust in this quad- 
rangle had never suffered the disturbances which are evidenced 
by the complex faulting, the Bethel sandstone would have con- 
stituted a continuous belt from one to two miles wide, extending 
from the southeastern corner of the quadrangle to the western 
border, about four miles south of the northwest corner. As it 
exists today the outcrop of the formation is restricted for the 
most part to this belt, just southwest of the major northwest- 
southeast lines of faulting, but it is offset to the east or to the 
west a number of times by the east-west faults which cross the 
quadrangle, so that the total width of the belt in which the out- 
crop is included is considerably greater than it would have 
been otherwise. The pattern of the outcrop is made very irregu- 
lar through this belt by reason of the effects of stream erosion. 

Tithelogic characters. As it is exposed in surface outcrop 
in the Princeton Quadrangle, the Bethel sandstone is commonly 
light brown in color, moderately fine grained in texture, and 
more or less friable in character. Much of the formation is 
massively bedded with much cross bedding, but locally it is 
thinly and evenly bedded. If the sandstone were encountered 
under cover, as in well drilling, the sand might be expected to 
be less oxidised and somewhat lghter in color. It is probably 
the coarsest in texture of any of the sandstone formations of 
the Chester Series in this area, it is aS massive as any of the 
others, although some of the beds in the Tar Springs and also 
the Palestine sandstones are as massive. 


°* Paper read before Geol, Soc. Amer., but not published. 
‘Ky. Geol. Surv., Miss. Form. West. Ky., p. 63 (1917). 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 41 











A THRUST FAULT IN THE BETHEL SANDSTONE. 


The small fault may be seen in Walche’s Cut, Illinois Central Railroad, 
east of Scottsburg. 


Thickness. The usual thickness of the Bethel sandstone 
about Princeton is about 40 feet, but in one locality at least, 


two and one-half miles east of the town, there is a thickness of 
only 25 feet. 


42 PRINCETON QUADRANGLE 


Stratigraphic relations. Presumably the Bethel sandstone 
lies unconformably upon the underlying Renault limestone. 
The actual contact between the two formations is best exhibited 
in the Quadrangle, in Walche’s cut on the new line of the 
Illinois Central Railroad, northeast of Scottsburg. The two 
formations are exposed west of the bridge crossing the cut, the 
sandstone at this locality being more thinly bedded than usual. 
Throughout a part of the section the sandstone apparently rests 
upon a massive, cherty limestone member of the Renault, but 
elsewhere there is a laver of variegated clay shale between it 
and the same cherty lHmestone bed, a condition which suggests 
the removal, in places, of the shale before the sandstone was 
deposited. In Hardin County, Dlinois, the contact between 
these two formations is well exhibited in the Ohio River bluffs * 
and clearly shows the unconformity between them, and it is 
not unlikely that this unconformity continues to the Princeton 
Quadranele. 

The contact between the Bethel and the overlying Paint 
Creek formation has not been observed. There seems to be an 
abrupt change from the sandstone into the overlying limestones 
and shales, which suggests a condition of unconformity, and 
there is some evidence of unconformable relations at this horizon 
in Hardin County, Iimois. However, with the present infor- 
mation available it is not possible either to affirm or deny such 
an unconformity in the Princeton Quadrangle. 

Paleontology. No fossils of importance have been detected 
in the Bethel sandstone in the Princeton Quadrangle, although 
in places there are fragments of undeterminable plant remains 
such as are found in the formation throughout its extent in 
Kentucky and Illinois. 

Correlation. The Bethel sandstone has been traced and 
mapped in detail from the Princeton Quadrangle in Kentucky, 
to near Anna, Union County, Illinois. The formation thins 
materially towards the western portion of its outerop in Ilinois, 
and in at least one, and perhaps in other localities of small ex- 
tent, it is absent altogether, permitting the Paint Creek to rest 
upon the Renault. The continuity of the bed throughout the 
whole distance, however, is unquestioned. The formation is said 


TI, State Geol. Surv., Bull. No... 41) pp, 146-147-971). 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 43 








by Butts to continue eastward from the Princeton Quadrangle 
to near Fairview, close to the line between Christian and Todd 
Counties, Kentucky, but, according to the same author, it has 
not been observed farther east.§ 

Tn the Mississippi River sections of the Chester Series, the 
position of the Bethel sandstone is occupied by the Yankeetown 
formation, a thin, siliceous bed which is in part chert, and locally 
a quartzite. 

in Breckenridge County, Kentucky, Butts has described 
the Sample sandstone, assigning it to a position supposed to be 
higher in the Chester Series than that occupied by the Bethel.?® 
There seems to be no doubt, however, that the Sample is the 
exact equivalent of the Bethel, and consequently the name 
Sample should be abandoned. The relationship of the Bethel and 
Sample sandstones will be discussed more fully on a later page, 
in connection with the consideration of the Paint Creek forma- 
tion, and the so-called Gasper limestone of Butts. 


PAINT CREEK LIMESTONE 


Name. This formation was originally described from Mon- 
roe and Randolph Counties, Illinois, the name being taken from 
a stream in southern Monroe County. The formation has been 
recognized and mapped in detail across these Mississippi River 
counties in Illimois and southward across the Mississippi River 
into Perry County, Missouri, also across the southern counties 
of Illinois from Union to Hardin, and across the Ohio River 
into Livingston, Crittenden and Caldwell Counties, Kentucky. 

When Ulrich first described the Chester section of western 
Kentucky, he defined the Tribune limestone as a formation with 
oolitic beds, overlying the Bethel sandstone, which he at that 
time called the Cypress sandstone. The formation was named 
from outcrops at Tribune, six miles east of Marion, which have 
been shown by the writer to belong far up in the Chester section, 
really being a part of the Menard limestone.!° Another of the 
original Tribune localities specified by Ulrich is the limestone 
outcrop at the mouth of the Fairview Mine at Rosiclare, [linois, 








Pee Gol Sit...) Miss, sHOrn?.. NV. iy, p63 G9lDz 

Ve cola puny as ky... IVLISS.) Eh Oormin awe ky") p: WH: oly) 

10 Paper read at the Washington Meeting of Geol. Soc. Amer., but not 
published. (1915). 


44 PRINCETON QUADRANGLE 





and this limestone has been shown by the writer to be the 
Renault.11 Still another of the specified localities for the Tri- 
bune limestone, designated by Ulrich is in Livingston County, 
Kentucky, east of Jov. Detailed mapping of this region has 
shown that no limestone of any sort is present at the locality 
indicated, and that it is situated in the midst of an unbroken 
area of Cypress sandstone. 

In his later contributions Ulrich !2 has indicated that what. 
he really intended to designate as Tribune is certain limestone 
exposures between Princeton and Hopkinsville, at about the 
line between Caldwell and Christian Counties, which are just 
a little east of the Princeton Quadrangle, and beds at another 
exposure east of Scottsburg which are in the Princeton Quad- 
rangle. The limestones at both of these two localities are the 
aint Creek of this report. 

An attempt has been made by Butts to eliminate the con- 
fusion introduced by Ulrich by his naming of a formation 
defined as overlying the Bethel (Cypress of Ulrich) sandstone, 
from outcrops at Tribune which occupy a very different strati- 
eraphie position, by the proposal of the name Gasper ?* as a 
substitute for Tribune, a substitute accepted by Ulrich. As 
used by Butts and Ulrich the Gasper includes not only the 
‘‘Tribune’’ east of Princeton, which is the exact equivalent of 
the Paint Creek, but also beds which are clearly the exact equiva- 
lents of the Renault, the Sample sandstone member of the Gas- 
per in Breckenridge County, being really nothing else than the 
more eastern manifestation of the Bethel sandstone. The intro- 
Cuction of the name Gasper, therefore, has not clarified the 
situation in the least. The Paint Creek of southern Illinois 
is clearly the exact equivalent of the beds in western Kentucky 
to which Ulrich intended to apply the name Tribune, and even 
if the Gasper were the exact equivalent of Ulrich’s earlier name 
it would he ruled out by the prior name Paint Creek. 

Distribution. In the Princeton Quadrangle the surface 
exposures of the Paint Creek formation are confined in general, 
to the same northwest-southeast belt in which the Renault and 

STS Stave Geols Surv. > UN OsT4I-e Dme oom GlozinE 


aK y. .Geol, Suryvs) Miss SP orm..0W. is ¥ DD solo Cola 
4 Ky. Geol. Surv.s, Miss: Horm, .W. Ky. p.264°917): 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES: 45. 





Bethel are found. In his original description of the Tribune 
limestone, which properly interpreted, as already pointed out, is 
the exact equivalent of the Paint Creek, Ulrich says !* ‘‘The 
Tribune limestone rarely comes to the surface in the region: 
under discussion. Indeed it has been certainly recognized in: 
only six localities in the district, and at only five points in the’ 
area covered by the map accompanying this report.’’ Of the 
six localities named by Ulrich that at Tribune, Kentucky, is 
Menard limestone, that east of Joy is in the midst of the Cypress 
sandstone, and that at the Fairview mine at Rosiclare is Renault 
limestone. The locality at Lamb’s cut on the old line of the 
Illinois Central Railroad is the only one of the original localities: 
specified by Ulrich which lies within the limits of the Prinece- 
ton Quadrangle, and it does occupy the true position assigned 
to the formation. This Lamb’s cut outcrop, however, is really 
one of the less important of the Paint Creek outcrops in the 
Quadrangle, and there are many other excellent and abundantly 
fossiliferous exposures of the formation which were mapped as 
Birdsville by Ulrich. From this situation, therefore, it will 
be seen that Ulrich not only misidentified much of his so-called. 
Tribune, but also failed to recognize a great deal of limestone 
which he should properly have placed in the formation. 

The greater portion of the Paint Creek in the quadrangle 
hes to the southeast of Princeton. The areas of outcrop are 
somewhat scattered and discontinuous by reason of the extreme 
faulting, but the distribution is shown upon the accompanying” 
map. One area of considerable extent lies northwest of Prince-- 
ton, in the fault block bounded by faults 11, 28, 29, and 30. 


Tithologic characters. The Paint Creek is in the main a 
limestone formation with interbedded shale layers of varying 
thickness. Kverywhere in the quadrangle, where the formation 
is exposed, the outcrop is more or less covered with talus or’ 
residuum, so that the exact succession of beds in the formation 
cannot be determined. There seems to be a considerable num-- 
ber of limestone ledges with shale partings in the lower part 
of the formation, then a series of beds that are more shaly, with 
numerous fossils, and above this a third division which again. 


“Prot, waper, -U..S, Geol, Surv., No. 36, p.'s9 (1905). 


46 PRINCETON QUADRANGLE 





is made up of more or less massive limestone ledges interbedded 
with shale layers. Some beds in the lower part of the formation 
are oolitic in texture and carry a fauna including many small 
molluses, and some oolitie beds are present locally in other por- 
tions of the formation, but the formation, as a whole, is not 
nearly so much of an oolitic limestone as the reader of Ulrich’s 
original description of the Tribune limestone would be led to 
believe. Some of the limestone beds of the formation, especially 
some of those in the higher portion, are hard and dense, weather- 
ing with smooth surfaces, and closely resemble in their outcrop 
-gome of the Renault exposures, but in the main the Paint Creek 
limestones are more crystalline than the Renault, and crumble 
somewhat under conditions of weathering, so that the weathered 
surfaces are rougher and give a better opportunity for the 
growth of lichens and mosses, which are most generally absent 
from the Renault exposures. The greater amount of shale in 
the Paint Creek also produces more slumping and more talus 
covering than is present over much of the Renault outcrop. 

As the Paint Creek is developed in Livingston County, 
Kentucky, and across the Ohio River in the southern counties of 
Illinois, it is very largely a shale formation, much of the shale 
being black or greenish in color and very fissile in character. 
Some of the shales in the middle portion of the Paint Creek in 
the Princeton Quadrangle are entirely like those of the section 
near the Ohio River, a good exhibition of such a shale being 
along the publie highway between Cedar Hill and Scottsburg, 
just south of fault No. 70. The westernmost exposures of the 
Paint Creek in the quadrangle are about one and one-fourth 
miles from the western border, a little southeast of Good Spring 
School, and the exposure at this locality is composed of about 
as much limestone as is present elsewhere in the quadrangle, 
so that the transition from the more calcareous to the nearly 
complete shale facies of the formation must take place across 
Crittenden County for the most part. 

In the upper part of the Paint Creek formation there is 
locally at least, a thin, more or less calcareous sandstone layer, 
followed by a few feet of more calcareous beds, beneath the con- 
tinuous sandstone of the overlying Cypress formation. Some 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 47 





question might be raised as to whether the sandstone should be’ 
included in the Paint Creek, or whether the limestone should: 
be considered as a part of the Cypress, but it seems best to 
draw the line between the two formations above the highest 
limestone. This situation is best exhibited near Scottsburg, a. 
little southeast of the village. 


Thickness. The full thickness of the Paint Creek is not 
exposed continuously anywhere in the quadrangle, in such a 
manner as to permit its measurement, bed by bed, but at a num- 
ber of places the interval between the underlying Bethel and the 
overlying Cypress sandstones can be rather closely determined, 
giving a thickness of essentially 100 feet for the Paint Creek. 
There is probably very little variation from this thickness any- 
where in the Quadrangle. 

Stratigraphic relations. It cannot be certainly established 
whether the Paint Creek rests unconformably upon the Bethel 
sandstone or not. At no locality in the quadrangle has the 
actual contact between the two formations been observed. In 
southern Illinois there is some evidence suggesting the presence 
of an unconformity at this horizon, but the beds might be uncon- 
formable there and still be perfectly conformable at Princeton, 
Kentucky. ‘The presence of a thin sandstone bed in the upper 
part of the Paint Creek, followed by a recurrent bed of lime- 
Stone, suggests that there was some alternation of conditions 
in the region at the time of transition from the Paint Creek 
to the overlying Cypress, and that the stratigraphic succession 
is really uninterrupted. 

Paleontology. The Paint Creek is perhaps the most fos- 
siliferous formation of the entire Chester Series in the Prince- 
ton Quadrangle, at least the fossils are most favorably preserved 
for purposes of collecting. Most of the limestone beds of the 
formation are only sparingly fossiliferous, and the fossils present 
are indifferently preserved. Some oolitic beds, locally present, 
near the base of the formation, do contain many fossils which 
constitute a rather varied fauna containing numerous small 
molluscs among other things. The most fossiliferous portion 
of the formation is some of the calcareous shale beds with thin 
limestone layers, in the middle portion of the formation. Upon 


48 PRINCETON QUADRANGLE 


some glade-like exposures of these beds great numbers of very 
perfectly preserved fossils can be collected, belonging to many 
species of brachiopods, bryozoans, and pentremites. 

The best collection which has been made from the basal, 
oolitie limestone, has been made at the road corner just east 
of the Hopkinsville branch of the Hhnois Central Railroad, a 
little over one-half mile northwest of McGowan Station. 

The largest collection which has been made from the eal- 
eareous Shale layers near the middle of the Paint Creek forma- 
tion, is from a rather extensive glade about one-fourth mile 
north of the Sand Lick Road, a little more than one-fourth mile 
from the east boundary of the quadrangle. The species which 
have been identified are as follows: 


Paint Creek Fauna from North of Clay Lick Road 
Triplophyllum spinulosum (M.-H. & H.) 
Amplexus sp. 

Michelinia sp. 

Pentremites pyriformis Say. 

Pentremites godoni de France. 
Pentremites sp. (godoni Ulrich, not de France). 
Mesoblastus cf. incurvatus Weller. 
Pterotocrinus sp. (wing plates). 
AGJQ@SSiZOCcrinus sp. 

Taxrocrinus sp. 

Crinoid stem (pentagonal). 

EHridopora punctifera Ulrich. 

Stenopora cestriensis Ulrich. 

Anisotrypa symmetricus Ulrich. 

Polypora sp. 

Cystodictya labiosa Weller. 

Crania chesterensis Miller and Gurley. 
Schuchertella costatula (Hall and Clarke). 
Orthotetes kaskaskiensis (McChesney). 
Chonetes chesterensis Weller. 

Productus inflaius McChesney. 

Productus ovatus Hall. 

Productus sp. 

Productus cf. parvulus Meek and Worthen. 
Diaphragmus elegans (N. & P.). 
Camarotecechia purduei Girty. 

Dielasma illinoisensis Weller. 

Girtyella brevilobata (Swallow). 

Girtyella indianensis (Girty). 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 49 





Spiriferina transversa (McChesney). 
Spiriferina spinosa (N. & P.). 
Spirifer increbescens var. transversalis Hall. 
Spirifer sp. 

Reticularia setigera (Hall). 
Eumetria vera (Hall). 
Cliothyridina sublamellosa (Hall). 
Composita trinuclea (Hall). 
Conocardium sp. 

Bellerophon sp. 

Platyceras sp. 

Phillipsia sp. 

Fish tooth. 


Many other smaller collections have been made from the 
shale beds at essentially the same horizon as the fauna recorded 
above, but as they all duplicate the above list to.a greater or 
less extent, it will be unnecessary to present lists. 

Correlation. A comparison of the fauna of the Paint Creek 
beds in the Princeton Quadrangle, with that of the same forma- 
tion as far away as Monroe and St. Clair Counties, Illinois, shows 
very much in common. The formation is peculiarly the horizon 
of Cystodictya labiosa, a species which is present in great 
abundance. This bryozoan also does occur in the fauna of the 
Renault limestone, but never in such great numbers as in the 
Paint Creek. The species is unknown outside of these two 
formations. This formation in the Princeton Quadrangle is 
likewise a horizon of great abundance of Pentremites, and while 
there is some geographic variation exhibited by the members 
of the genus Pentremites in passing from place to place, there 
is a notable community of forms in the Paint Creek of the 
Princeton Quadrangle and that of the Mississippi River coun- 
ties in Hlinois. Chonetes illinoisensis, described, originally from 
a Paint Creek fauna in St. Clair County, Illinois, is the only 
Chester species of the genus in western Illinois, and is known 
only from this horizon. In the Princeton Quadrangle it is like- 
wise present, being the only Chester species of the genus, and 
it occurs only in this formation. 

In their more recent writings both Butts and Ulrich 15 have 
used the name Gasper in place of Tribune, because of the unfor- 


1 Ky. .Geol. Surv., Miss. Form. West. Ky. 


50 PRINCETON QUADRANGLE 


tunate choice of the latter name. The typical Tribune is the 
same as the Paint Creek of the Princeton Quadrangle, but the 
typical Gasper is exposed farther east in Kentucky than the 
Princeton Quadrangle, and as described consists of two lime- 
stone members separated by the Sample sandstone member. The 
whole of the more typical Gasper is correlated by these authors 
with the Renault and Paint Creek limestones together of the 
western Illinois section, a correlation which seems to be wholly 
justified. The same authors consider the Paint Creek of the 
Princeton region to be the equivalent of the whole of the Gasper 
farther east, and consequently must find the equivalent of the 
Sample sandstone member within the 100 feet of the formation. 
In western Christian County, along the Prineceton-Hopkinsville 
Pike, ‘‘Ulrich’s type locality of the Tribune limestone,’’ Butts 1° 
has designated a clay bed two to three feet thick as the equivalent 
of the Sample sandstone of Breckenridge County, and in this 
manner he is able to make two divisions of the Gasper such as 
are present in the more typical section. There is no reason 
whatsoever for dividing this ‘‘typical Tribune limestone’’ sec- 
tion, so far as the paleonthological evidence is concerned, and 
the whole interpretation is based on the misconception of the 
true relationship of the Sample anl Bethel sandstones, which 
are really exactly equivalent. In Breckenridge County the true 
Renault fauna is present beneath the Sample sandstone just 
as it is present beneath the Bethel sandstone in the region east 
of Princeton, and the Paint Creek fauna is present in beds 
overlying these two sandstones in the two regions. Both Butts 
and Ulrich have assumed without reason that the ‘‘Upper 
Ohara’’ in the Princeton region is older than the Renault, there- 
fore it is necessary for them to find some equivalent for the 
Renault in the formation they now call Gasper. The same men 
have recently determined that the Renault (‘‘Upper Ohara’’) 
in Union County, Hlinois, is Paint Creek in age,!* a determina- 
tion which is proven to be incorrect by reason of the beds having 
been actually traced and mapped in detail from the undisputed 
‘‘Upper Ohara’’ farther east in Illinois, to the outcrop which 
they examined in Union County. 


as Ky. Geol Sury., Miss, gE Orm: » West K Yu) Doles 
Bull? ‘Geol Soc. Amer, vol. e335 pe 832e C1922). 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 51 





Both paleontological and stratigraphical evidence confirm 
the exact correlation of Ulrich’s ‘‘Tribune limestone’’ of the 
section east of Princeton, with the Paint Creek formation of 
southern and southwestern Illinois, and with the upper division 
of the Gasper limestone of Breckinridge County, Kentucky. 

One of the species which has been enumerated in the Paint 
Creek faunal list recorded on an earlier page, is Camarotoechia 
purduet. This is a rhynchonelloid brachiopod shell, a type 
which is unusual in the Chester fauna of southern Illinois and 
western Kentucky, and which is wholly unknown in most of 
the formations. In the locality where it has been found the 
Species occurs in great numbers. It was originally described 
from the Moorefield shale of Arkansas, a Chester formation 
which has never been correlated with entire satisfaction with 
the Chester formations of the Illinois basin. The great abun- 
dance of the species in this Kentucky Paint Creek fauna sug- 
gests, at least, the correlation of the Moorefield with the Paint 
Creek. During the summer of 1920 a single specimen of 
Tnorhynchus carboniferum, another species peculiar to the 
Moretield shale of Arkansas, was collected by the writer in Liv- 
ineston County, Kentucky, from a limestone bed which was 
believed to be Golconda in age, suggesting the correlation of the 
Moorefield with the Golconda formation. From paleontological 
evidence at hand at the present time, the correlation of the 
Moorefield with either the Paint Creek or the Golconda, or per- 
haps with both these formations, can be assumed, but more cer- 
tain determination of the age of the Arkansas formation must 
await additional knowledge of fossil faunas in Kentucky. 


CYPRESS SANDSTONE 

Name. This is not the Cypress sandstone of Ulrich’s orig- 
inal report on western Kentucky, which, as has been shown, is 
in reality the Bethel sandstone. The Cypress was originally 
deseribed by Engelmann from Cypress Creek in Union County, 
Illinois, and the formation has now been traced and mapped in 
detail clear across southern Illinois and into Kentucky. It is 
the formation which lies above the Paint Creek (Ulrich’s orig- 
inal Tribune limestone), instead of the sandstone beneath it. 
In some parts of western Kentucky the Cypress is the bed which 


UNIVERSITy OF 
ILLINOIS LIBRARY 


52 PRINCETON QUADRANGLE 





Ulrich designated as bed No. 1 of the Birdsville, but, as will be 
shown, much of this Birdsville No. 1 is really the Tar Springs 
sandstone, occupying a much higher position in the section. 


Distribution. Because of its limited thickness the Cypress 
is a much less important sandstone formation in the Princeton 
Quadrangle than it is farther west in Kentucky and in southern 
Illinois. Jike the already described Chester formations its area 
of outcrop is in the belt extending to the northwest from the 
southeastern corner of the quadrangle, southwest of the main 
line of faulting The most extensive outcrops are south and 
southeast of Scottsburg, but it is also present along and west 
of the Farmersville road four miles northwest of Princeton. 
Some of the best exposures of the formation are present in the 
road between Scottsburg and Friendship. 

Tithologic characters. The Cypress is a thinly bedded 
sandstone in the Princeton Quadrangle, of rather fine texture, 
the surfaces of the layers bearing ripple marks and other mark- 
ines of shallow water conditions. The sandstone is commonly 
brown in color, or yellowish in some places. 

Thickness. The total thickness of the Cypress sandstone 
has nowhere been observed fully exposed in the Princeton Quad- 
rangle, in such a condition that it can be accurately measured. 
In the section at Walche’s cut there are 30 feet of Cypress 
exposed, but the exposure is interrupted by a fault on the west, 
and the total thickness should probably be somewhat greater. 
The best locality for observing the extent of the interval between 
the top of the Paint Creek and the base of the overlying Gol- 
conda formation, is about a mile southeast of Scottsburg, and 
while the limits of the two bounding formations cannot be 
accurately fixed, the interval is clearly less than 40 feet, and 
the Cypress is probably about 380 feet thick at this place. 
Nowhere in the quadrangle is there any evidence that the for- 
mation exceeds 40 feet in thickness. 

In his deseription of a ‘‘Section of the Chester Series in 
Caldwell County, east of Princeton, Ky.,’’ Ulrich!® has 
described the Cypress as a series of beds 163 feet in thickness, 
with 124 feet more as questionably Cypress, making 287 feet 








wikhy. Geol. Surnv.; -Miss: “Norm: “West. ik y., «pee i-16- 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 53 








STEEPLY INCLINED CYPRESS SANDSTONE 


This view is in Walche’s Cut, Illinois Central Railroad, east of Scotts- 
burg, Caldwell County, Kentucky. 


in all. This shows an utter misconception of the Chester sec- 
tion of the region on his part, and the sandstones which he has 
described, so far as he has described anything, belong to the 
Tar Springs formation rather than the Cypress. Indeed, the 
whole of Ulrich’s so-called Birdsville bed No. 1 in the Princeton 
area, which should be the Cypress sandstone in accordance with 
his present conception, is Tar Springs sandstone, although the 
Birdsville No. 1 farther west, towards the Ohio River, is really 
the Cypress. 

Stratigraphic relations. The stratigraphic relations of the 
Cypress with the underlying and overlying formations is not 
entirely clear in the Princeton Quadrangle. As has been indi- 
cated already, the alternation of thin limestone and sandstone 
members at the horizon of transition from the Paint Creek to 
the Cypress, especially as exhibited southeast of Scottsburg, 
suggests the absence of any relation of unconformity at the 
base of the formation. No unconformity between the Cypress 
sandstone and the overlying Golconda formation has been cer- 
tainly established in the Princeton Quadrangle, although an 
unconformity at this horizon is widely present farther west in 
Kentucky and in southern Illinois. 


54 PRINCETON QUADRANGLE 





Paleontology. No fossils of any sort have been observed 
in the Cypress sandstone in the Princeton Quadrangle, although 
it would not be unexpected to find fragments of plant remains, 
especially broken trunks of Lepidodendron. 


Correlation. The correlation of the Cypress sandstone in 


the Princeton Quadrangle is established by its stratigraphic. 
position between the certainly determined overlying and under- | 


lying formations on the basis of their contained fossils. These 
formations are unquestionably the Paint Creek below and the 
Goleonda above, which establishes the position of the inter- 
veninge sandstone as being the same as that of the typical 
Cypress sandstone in southern Illinois. 


GoLCONDA LIMESTONE 


Name. The Goleonda formation has been named from 
excellent exposures in the Ohio River bluffs above the town of 
Golconda, Illinois. The name has been carried over into Liy- 
ingston County, Kentucky, in the detailed mapping of the 
Goleonda quadrangle, and it has been mapped in detail across 
‘much of Crittenden County. The presence of the formation in 
the Princeton quadrangle has been fully established by the 
fossil collections which have been secured. 

Distribution. The Golconda is nowhere the surface for- 
mation under any considerable area within the Princeton quad- 
rangle, although it is distributed in more or less isolated out- 
crops almost entirely across the quadrangle within the much 
faulted helt. The most extensive area of outcrop of the forma- 
tion, within the limits of the quadrangle, is east of Scottsburg, 
between faults Nos. 74 and 76. The actual exposures in the 
area are really few, the best exhibition of the formation being 
three-fourths of a mile southeast of Scottsburg, and one-tenth 
of a mile northeast of the public road to Friendship, where the 
characteristic fossils of the formation can be collected in abun- 
dance. The formation must underlie the surface traversed by 
the Sand Jick road for three-fourths of a mile southeast from 
the crossing over the old line of the Illinois Central Railroad, 
but the actual exposures are limited to a few limestone ledges, 
more or less displaced, a little over one-half mile from the 


STRATIGRAPHIC GEHOLOGY—CHESTER SERIES 55 





railroad crossing. Excellent exposures of some of the shale 
beds of the formation are present in the upper portion of the 
valley crossing the boundary between Otter Pond and Claxton 
rectangles, a little less than one and one-half miles west of the 
quadrangle boundary. Elsewhere within this area the presence 
of the Golconda is indicated by the low and flat topography 
and by the attitude of the overlying sandstone. 

In the southeastern part of the Claxton rectangle the Gol- 
econda formation outcrops in the block bounded by faults 64, 
65, 66, 70, and 45. The formation is present in the southern 
portion of this block, and is best exposed in the southwestern 
portion adjacent to fault No. 45, where the beds are steeply 
inclined, and have furnished a large and characteristic fauna. 
A narrow outcrop of the formation extends longitudinally 
through the middle of the fault block bounded by faults 57, 62, 
63 and 45, the best exposure along this hne being in Walche’s 
cut, near its western extremity. A number of outcrops of the 
Goleonda are present near the line between the Princeton and 
Claxton rectangles, over a distance of one and three-fourths 
miles north from the main road from Princeton to Dawson 
Springs. Along this belt the outcrops are really present in four 
distinet fault blocks, although there is no great dislocation 
between the different areas. 

From three and one-half to four and one-half miles north- 
west of Princeton, near the road to Farmersville, the Golconda 
presents a narrow, band-like outcrop in the fault block bounded 
by faults 16, 17, 28, and 11. The best outcrops in this belt are 
in the southeastern part of the fault block. Other outcrops are 
present in the narrow, tilted fault block lying between faults 
3 and 9 in the Flat Rock rectangle. 

lithological characters. Throughout the Princeton quad- 
rangle, the Goleonda is much more of a shale formation than a 
limestone, although in nearly every locality where the forma- 
tion has been observed there are thin limestone layers inter- 
ealated in the shale. The shales differ more or less in character 
from place to place. In Walche’s cut, nearly the whole forma- 
tion is made up of black, fissile shale, elsewhere the shales are 
lighter in color, and in places they are more or less siliceous 
with some sandy layers. The limestone layers are also variable 


56 PRINCETON QUADRANGLE 





~ in character, but they are for the most part crystalline in tex- 
ture, and vary from dark to lght gray and brown in color. 
The beds are commonly thin, a foot more or less, and the maxi- 
mum thickness observed is not over six feet. 

In a number of the Golconda exposures which have been 
observed, there is a layer of hard limestone conglomerate, with 
some chert pebbles in places. This conglomerate bed does not 
occur at the base of the formation, but is commonly. somewhere 
near the middle. In Walche’s cut it is ten inches thick, and 
a similar thickness has been observed in a number of other 
localities. Its maximum development, so far as seen, is in a 
eut on the old line of the Illinois Central Railroad, where there 
are really two layers of the conglomerate separated by sand- 
stone, the whole thickness beine about five feet. Where weath- 
ered the conglomerate layer is more or less ferruginous, and 
commonly contains worn fossils, which in places are numerous. 

Thickness. The maximum thickness of the Golconda for- 
mation, as it has been observed in the Princeton quadranele, is 
80 feet in the Walche’s cut section. In some other places it 
cannot exceed 50 feet in thickness, and 1s even as thin as 30 
feet in some of the sections studied. In the Walche’s cut 
section over 60 feet of the entire thickness is black, fissile shale, 
in the midst of which is the conglomerate layer. The basal 
portion of the formation at this locality is a hard limestone. 

Ulrich 1° has described the Goleonda formation east of 
Princeton as a limestone with thick and thin shale partings with 
a thickness of 50 feet. He also expresses the opinion that some 
124 feet of beds which are arenaceous in the main and which 
are believed by him to underlie the limestone and shale beds, 
are perhaps the equivalent of the lower portion of the Goleonda 
as the formation is developed in its typical exposures. These 
arenaceous beds, however, are in fact a part of the Tar Springs 


formation and belong far above the Golconda in the Chester 
section. 


Stratigraphic. relations. In all probability the Goleonda 
formation follows the Cypress sandstone without stratigraphic 
interruption. In Walche’s cut most of the upper ten feet of 


” Ky. Geol, Surv., Miss. Form. West. Ky., pp. 73-74. 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 57 


the Cypress is thinly bedded. At the very top of the forma- . 
tion there is a three-inch layer of thinly laminated gray sand- 
stone, followed by six inches of rusty, siliceous limestone. This 
limestone is followed by 18 inches of dark gray, carbonaceous 
shale which in turn is succeeded by 5 feet 11 inches of massive, 
eray, erystalline limestone. This succession seems to indicate 
that there may have been a somewhat gradual change in the 
character of sediments, from the arenaceous Cypress to the eal- 
eareous and shaly Goleonda. In general, throughout the Ohio 
Valley, there seems to be no stratigraphic break in the section, 
and the chances are that the same conditions exist in the Prince- 
ton quadrangle. On the other hand, unconformity at the top 
of the Goleonda has been clearly recognized at a number of 
localities in the Ohio Vallev, both in western Kentucky and in 
southern I]linois, and although such a relation has not been 
certainly established in the Princeton quadrangle, the varying 
thickness of the Goleonda suggests that such may be the situa- 
tion. Furthermore it is established by the fossil faunas that it 
is the lower portion of the Goleonda which is present in the 
cnuadrangle, a situation which would favor the absence of uncon- 
formity between the formation and the underlying Cypress. 

Paleontology. Good fossils have been collected at a number 
of localities in the Princeton quadrangle. In the four principal 
areas of outcrop of the formation, the characteristic basal Gol- 
econda species, Pterotocrinus capitalis, has been found. Two 
distinct faunal assemblages have been recognized, one with the 
usual brachiopods, bryozoans and P. capitalis, the assemblage 
which is very characteristic of the basal Goleonda from the 
Princeton quadrangle to Union County, Illinois. The second 
fauna is a mollusean fauna with many bellerophontids and some 
peleeypods, among which is the peculiar Nucula platynotus, a 
fauna which has been recognized here in the Princeton quad- 
rangle, in Livingston County, Kentucky, in southern Johnson 
County, Illinois, and again in the basal Okaw limestone in Ran- 
dolph County, Tinois. 

The best representative collection of the usual Pterotocrinus 
capitalis fauna of the lower Golconda is from a locality three- 
fourths of a mile southeast of Seottsburg, where the following 
species have been recognized : 


58 PRINCETON QUADRANGLE 





Fauna of the Golconda Limestone Near Scottsburg 


Triplophyllum spinulosum (M. E. & H.). 
Pentremites sp. 7 
Pterotocrinus capitalis (Lyon). 
Pterotocrinus sp. (wing plates). 
Zeacrinus sp. 

EKupachyrinus sp. 

Echinoid spine. 

Fistulipora excellens Ulrich. 
Eridopora punctifera Ulrich. 
Eridopora macrostoma Ulrich. 
Meekopora clausa (Ulrich). 
Stenopora tuberculata (Prout). 
Fenestella cestriensis Ulrich. 
Fenestella elevatipora Ulrich. 
Archimedes communis Ulrich. 
Archimedes compactus Ulrich. 
Archimedes distans Ulrich. 
Archimedes intermedius Ulrich. 
Archimedes meekanus (Hall). 
Archimedes proutanus Uirich. 
Archimedes swallovanus (Hall). 
Archimedes terebriformis Ulrich. 
Reteporina flexuosa (Ulrich). 
Rhombopora tabulata Ulrich. 
Streblotrypa nicklesi Ulrich. 
Productus ovatus Hall. 
Diaphragqmus elegans (N. & P.). 
Camarophoria explanata (McChesney). 
Rhynchopora perryensis Weller. 
Dielasma illinoisensis Weller. 
Girtyella indianensis (Girty). 
Girtyella brevilobata (Swallow). 
Spiriferina transversa (McChesney). 
Spiriferina spinosa (N. & P.). 
Spirifer sp. 

Humetria vera (Hall). 
Cliothyridina sublamellosa (Hall). 
Composita trinuclea (Hall). 
Sphenotus cf. monroensis Weller. 
Euphemus randolphensis Weller. 
Orthoceras sp. 

Fish tooth. 


The best exhibition of the Nucula platynotus fauna is from 
a locality east of Sulphur Creek, one and one-fourth miles south- 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 59 


west of Claxton. <A collection from this locality has furnished 
the following species: 

Fauna of the Golconda Limestone Near Claxton 
Triplophyllum spinulosum (M.-E, & H.). 
Pterotocrinus capitalis Lyon. 
Pterotocrinus sp. 

Echinoid spine. 

Meekopora eximia Ulrich. 

Stenopora cestriensis Ulrich. 
Batostomella sp. 

Fenestella (several species). 
Archimedes intermcdius Ulrich. 
Archimedes lativolvis Ulrich. 
Archimedes terebriformis Ulrich. 
Polypora approximata Ulrich. 
Septopora cestriensis Ulrich. 
Rhombopora cf. tabulata Ulrich. 
Linguia sp. 

Glossina sp. 

Orbiculoidea sp. 

Orthotetes kaskaskiensis (McChesney). 
Productus ovaius Hall. 

Productus parvulus Winchell. 
Diaphragmus elegans (N. & P.). 
Girtyella indianensis (Girty). 
Spiriferina transversa (McChesney). 
Spiriferina spinosa (N. & P.). 
Spirifer increbescens var. transversalis Hall. 
Spirifer sp. 

Humetria vera (Hall). 
Cliothyridina sublamellosa (Hall). 
Composita trinuclea (Hall). 
Spenotus rectangularis Weller. 
Sphenotus (several species). 
Nucula randolphensis Weller. 
Nucula platynotus Weller. 

Leda sp. 

Parallelodon micronema (M. & G.). 
Conocardium chesterensis Weller. 
Schizodus depressus Worthen. 
Cypricardella oblonga (Hall). 
Bellerophon chesterensis Weller. 
Euphemus randolphensis Weller. 
Bucanopsis nodosus Weller. 
Laevidentalium cf. venustum (M. & W.). 
Plagioglypta sp. 


60 PRINCETON QUADRANGLE 


Ptychomphalus (several species). 
Mourlonia sp. 

Ivania sp. 

Murchisonia (several species). 
Bembewxia cf. conicus Weller. 
Huomphalus sp. 

Naticopsis sp. 

Zygopleura sp. 

Bulimorhpa sp. 

Platyceras sp. 

Orthoceras cf. okawense M. & W. 
Phillipsia sp. 


Smaller collections of Golconda fossils have been made 
from a number of other localities, but in every case they are 
of the usual species commonly found in the formation. 

Correlation. The fossil faunas from the Goleonda forma- 
tion which have been recorded above establish conclusively 
that the beds in the Princeton quadrangle represent the lower 
portion of the formation, since both of the two faunal groups 
which have been recorded are wholly restricted to this horizon 
so far as they are known. 

Ulrich 7° has expressed the belief that only the upper por- 
tion of the Goleonda formation, as it is developed along the 
Ohio River, is present in the Princeton region of Kentucky, 
and that the lower Goleonda is represented by a series of 124 
feet of beds chiefly arenaceous in character, the alternative 
interpretation being that these arenaceous beds are the upper 
part of the Cypress sandstone. As already stated, however, it 
has been shown that all of these sandstone beds, deseribed as 
Cypress or lower Goleonda by Ulrich, are really a part of the 
much higher Tar Springs sandstone. 

From the statements which they have made it seems doubt- 
ful whether either Ulrich or Butts have ever seen the Goleonda 
formation in the Princeton area. Jf either of them had ever 
visited any of the good outcrops which exist at various localities, 
they could not have failed to detect the characteristic Pteroto- 
crinus capitalis fauna, and if this fauna had been seen the mis- 
take of considering the lower Golconda absent or represented 
by a series of sandy beds could not have been made. 


“Ky, Geol. Survo,e Missogrorm. “WestalKy:. Do ue: 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 61 





HARDINSBURG SANDSTONE 


Name. This formation was named by Butts 2! from out- 
crops in Breckenridge County, Kentucky. It has been recog- 
nized as a unit in the Chester Series throughout western Ken- 
tucky and across southern Illinois, even to Randolph County, 
where it is represented by local sandstone beds in the midst 
of the Okaw limestone.?? 

Distribution. The distribution of the Hardinsbure sand- 
stone in the Princeton quadrangle follows closely that of the 
underlying Goleonda formation. Wherever the Goleonda is 
exposed this sandstone is present overlying it, and in addition 
the formation is present in the northwestern portion of the 
Claxton rectangle along Lambs Creek, the excavation of the 
creek valley not being sufficiently deep to expose the Golconda. 
Another small outcrop where the Golconda is not present is 
south of Hazelhurst School, along the northeast side of fault 
No. 42. 

LTithologic characters. In the Walche’s cut section the 
Hardinsbure formation is largely shale, much of which is 
arenaceous, but associated with it are some calcareous bands. 
The lowermost bed, 9 feet 3 inches thick, is a more or less mas- 
sive sandstone with some thinly laminated shaly sandstone 
layers. Above the sandstone is a 10-inch layer of impure, 
siliceous limestone, and 18 feet 6 inches higher in the section 
is another similar limestone laver 7 inches thick. The remainder 
of the formation is shale, a’ part of which is interbedded with 
sandstone lavers one-half to three inches thick. The higher 
portion of the formation has a number of thin siliceous lme- 
stone layers interbedded with the nearly black shales, the 
highest portion of the formation becoming somewhat more 
calcareous. 

The formation as a whole is so shaly that it is commonly 
nearly hidden with talus, and this character, associated with the 
shaly nature of the underlying Golconda, does not permit the 
development of good exposures in the hillsides where the forma- 
tion is known to be present. The basal, more massively sandy 
portion of the formation seems to be considerably thicker in 


Ky, Geol. Surv., Miss: Form, West. Ky., p: 96 
2-Weller, Jour. Geol., Vol. 28, p, 301 (1920), 


62 PRINCETON QUADRANGLE 





some places than it is in Walche’s cut, and where this condition 
exists there are better exposures of it.- One of the best exposures 
of these sandstone beds which has been observed in the Princeton 
quadrangle is one and one-half miles east of Seottsburg, along 
the crossroad: connecting the Princeton-Hopkinsville pike with 
Sand Lick road. There are also some fair exposures of the 
sandstone, more thinly bedded, than along ‘the road last men- 
tioned, alone the western face of the hill lying between this 
road and Scottsbure. . 

Thickness. The thickness of the interval considered as 
Hardinsbure in the Walche’s cut section is 61 feet 1 inch, but 
this is probably greater than the interval between the Golconda 
and Glen Dean formations in some other parts of the quad- 
rangle. In some places the formation certainly does not exceed 
40 feet, and it may be as thin as 20 feet in some places. There 
is always much uncertainty concerning the exact thickness of 
the formation beeause it is rarely well exposed, and the only 
section where its exact limits can be seen is in Walche’s cut. 

Stratigraphic relations. The stratigraphic relations of the 
Hardinsburg sandstone with the underlying Golconda formation 
have already been considered. Neither the presence nor the lack 
of an unconformity at this horizon can be established in the 
Princeton quadrangle, although it is quite certain that the 
Hardinsburg rests unconformably upon the Golconda in Livy- 
ingston County, Kentucky, and across southern [hnois. 

There seems to be no evidence whatever for considering 
that there was any interruption in sedimentation in passing 
from the Hardinsbure to the Glen Dean limestone. The shales 
of the Hardinsburg become more calcareous in their upper por- 
tion and pass over into the limestone beds of the lower Glen 
Dean. 


Paleontology. In the higher portion of the beds which 
have been referred to the Hardinsbure formation in Walche’s 
cut, the caleareous lavers are fossiliferous, but the fossils are 
all poorly preserved and no attempt has been made to secure 
a representative fauna. No fossils at all have been observed 
in the sandstone beds of the formation, but fragmentary plant 
remains might be expected to occur. 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 63 








Correlation. The correlation of the Hardinsburg sandstone 
has been established by the actual tracing of the formation, 
between the overlying and underlying limestones, throughout 
the region of its occurrence. Its lithologiec characters change 
from place to place, but it is more or less of an arenaceous for- 
mation throughout, occupying the same stratigraphic position 
from Breckenridge County, Kentucky, to the Mississippi River. 


GLEN DEAN LIMESTONE 


Name. Butts named the Glen Dean limestone from expo- 
sures in Breckenridge County, Kentucky. The formation has 
been recognized wherever the Chester section has been carefully 
examined in western Kentucky, and it has been traced across 
southern Illinois to the Mississippi River. 

Distribution. In the Princeton quadrangle the Glen Dean 
formation is closely associated with the underlying Hardinsburg 
and Golconda formations. In every one of the fault blocks 
where the Goleonda is exposed the Glen Dean is also present, 
and in addition it is present in a number of places where the 
Golconda is not exposed. The most important of these latter 
outcrops is along Lamb’s Creek between faults 33 and 50, where 
the Glen Dean forms the valley floor for much of the distance, 
but in the more northern portion of the stream’s course, south of 
fault No. 33, the valley has been cut through the Glen Dean into 
the Hardinsbure, so that the Glen Dean itself outcrops on the 
valley sides. Throughout this Lamb’s Creek valley, as else- 
where, the actual exposures of the Glen Dean are not common. 
The shaly character of the formation itself, associated with the 
shaly character of the two underlying formations, Hardinsbure’ 
and Golconda, and with the presence of a massive, basal sand- 
stone bed in the lower part of the overlying Tar Springs forma- 
tion, furnish a combination of conditions which tend to obscure 
the Glen Dean outcrop nearly everywhere. The most con- 
tinuous exposure of the formation is in Walche’s cut. The best 
exposures seen elsewhere are northeast of Princeton, near the 
road to Lewistown. In one tributary to Lamb’s Creek from the 
west, just north of the Princeton-Lewiston road, one and one- 
half miles from Lewiston, the formation is well shown, but in 
other parts of the Lamb’s Creek outcrop actual exposures are 





64 PRINCETON QUADRANGLE 


scanty. Another good exhibition of the formation is along a 
narrow belt one-fourth mile long, extending southward from the 
same Princeton-Lewistown road, a little less than two miles 
southwest of Lewistown. This last outcrop Hes between faults 
48 and 49. 





A, PORTION OF THE GLIUN WHAN. 


This massive limestone member in the lower portion of the Glen Dean 
formation may be seen in Walche’s Cut, Illinois Central Railroad, east 
of Scottsburg, Caldwell County. 


Lithologic characters. The larger portion of the Glen Dean 
formation in the Princeton quadranele is shale, but at the base 
of the formation there is a massive limestone ledge, which in 
the Walche’s cut section is 10 feet 11 inches thick. This bed is 
believed to be persistent throughout the area and of about uni- 
form thickness. It is a very hard, tough limestone, somewhat 
crystalline, but in part compact and dense, gray in color. Fol- 
lowing the basal limestone in Walche’s eut there are 50 feet 
9 inches of black, carbonaceous, fissile shale. This in turn is 
followed by 4 feet 4 inches of thinly bedded sandstone, then 
2 feet, 8 inches of limestone. The next bed is 5 feet 2 inches 
of fine black fissile shale with a thin band of calcareous sand- 
stone near the top. The uppermost, 13 feet 2 inches, consists of 
impure, gray limestones interberred with shales, the individual 
beds being from two inches to two feet in thickness. At no 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 65 
other locality in the quadrangle is the complete suecession of 
beds in the Glen Dean exposed, but the lithologic character of 
the formation is somewhat uniform throughout the area. Wher- 
ever the formation is best exposed it is represented by more or 
less tumbled masses of limestone, which evidently are from the 
basal bed, and above these is a talus covered slope which 1s 
underlain by the more shaly portion of the formation. 

Thickness. The measured section of Glen Dean in Walche’s 
eut gives a total thickness of 87 feet, but this seems to be exces- 
sive when compared with the interval in other sections which 
can be occupied by the formation. About 40 feet seems to be 
the more usual thickness and in some places it seems to be even 
thinner than this. 

Stratigraphic relations. There seems to be no distinct 
interruption of sedimentation in passing from the Hardinsburg 
sandstone below, into the Glen Dean. Interbedded with some 
of the sandy shales which constitute the upper part of the 
Hardinsbure, there are thin beds of impure limestone, showing 
that the conditions favored .imestone sedimentation before the 
accumulation of the first massive bed of limestone which is 
considered as the base of the Glen Dean. Above the top of the 
formation there is an abrupt change from the shale and lime- 
stone sediments to the massive basal bed of the Tar Springs, 
and it is possible that the change may mean the presence of 
an unconformity, although such a relation cannot be certainly 
established from the observations in the Princeton quadrangle. 
The varying thickness of the Glen Dean formation, which seems 
to exist in the quadrangle, suggests that there may have been 
an interval of erosion preceding the deposition of the Tar 
Springs sandstone, which has removed a part of the Glen Dean 
in some places. Huture observations may serve to confirm or 
establish the absence of an unconformity at this horizon, but 
at the present time the relation is uncertain. 

Paleontology. Fossils are not abundant in the Glen Dean 
beds in the Princeton quadrangle, but in the interbedded lime- 
stone and shale member, at the top of the formation in Walche’s 
cut, the following species have been collected: 


66 PRINCETON QUADRANGLE 





Fauna of the Glen Dean Limestone in Walche’s Cut 

Amplexus ? sp. 

Pentremites brevis Ulrich. 

Pentremites canalis Ulrich. 

Pentremites sp. 

Hupachycrinus sp. 

Agassizocrinus sp. 

Pterotocrinus acutus Wetherby. 

Fistulipora excelens Ulrich. 

Hridopora punctifera Ulrich. 

EHridopora cf. macrestoma Ulrich. 

Cheilotrypa hispida Ulrich. 

Stenopora meekana Ulrich. 

Fenestella serratuia Ulrich. 

Fenestella tenax Ulrich. 

Archimedes intermedius Ulrich. 

Archimedes communis Ulrich. 

Polypora tuberculata Prout. 

Polypora approximata Ulrich. 

Lyropora sp. 

Septopora subquadrans Ulrich. 

Ptilopora sp. 

Rhombopora persimilis Ulrich. 

At one locality in the bed of Sulphur Creek, three-fourths 
of a mile southwest of Claxton, a ledge of massive lmestone 
belonging to the Glen Dean formation, possibly the basal bed, 
is covered with an abundance of imperfect and fragmentary 
examples of a large species of Pentremites which seems to be 
P. spvicatus, a characteristic Glen Dean species. At another 
locality in the bank of Lamb’s Creek just west.of fault No. 55, 
three-fourths of a mile southwest of Lewistown, there are ledges 
of Glen Dean limestone with an abundance of erinoid remains, 
amone which are numerous wing plates of Pterotocrinus acutus. 
In many of the Glen Dean exposures fossils are not conspicuous, 
and if present are poorly preserved and fragmentary. 

Correlation. The presence of such species as Pentremites 
brevis, Pentremites spicatus, and Pterotocrinus acutus, along 
with several of the species of bryozoans, is sufficient evidence 
for the determination as Glen Dean of the beds which have 
been so mapped in the Princeton quadrangle. These species are 
characteristic of this formation wherever they are known in 
western Kentucky and southern Illinois. Furthermore the 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 57 








stratigraphic position of the formation is that of the Glen Dean 
limestone, which has been traced and mapped in detail across 
the whole of southern Illinois and western Kentucky to the 
Princeton area. 


Tar SprRINGS SANDSTONE 

Name. The Tar Springs sandstone was so named by Owen 
in Breckenridge County, Kentucky. In that part of the State 
there are bitumen bearing springs emerging from the forma- 
tion, one of the largest of which is known as Tar Springs. In 
that county the formation overlies the typical Glen Dean lime- 
stone, and the name has been extended to the sandstone forma- 
tion throughout western Kentucky and southern Illinois, which 
overlies that formation. 

Distribution. Because of its greater thickness and the 
presence of more massive and less destructable sandstone beds, 
the Tar Springs sandstone occupies considerably larger areas 
than the three next older formations which are very largely 
shales in their composition. In some places in the Princeton 
quadrangle the Golconda, Hardinsburg and Glen Dean forma- 
tions together underlie more or less steeply sloping hillsides, 





BASE OF TAR SPRINGS SANDSTONE. 


-. The view is in Walche’s Cut, Illinois Central Railroad, east of Scotts- 
urg. 


68 PRINCETON QUADRANGLE 








and are capped by the more massive Tar Springs sandstone, 
which underlies much broader surfaces. 

The formation is well exposed in a number of fault blocks 
in the complexly faulted area south of. Claxton. Most of the 
more or less steeply dipping sandstone ledges in the several 
railroad cuts along the old line of the Illinois Central Railroad, 
a mile southwest of Claxton, are Tar Springs, and the hilltops in 
the fault block lying south of fault. No. 64 are of the same 
formation. 

The most continuous extensive area of outcrop of the for- 
mation is west and southwest of Lewistown, in several fault 
blocks which le in general between faults 33, 46, 45, and 55. 
The valley of Lamb’s Creek crosses this area in a general north- 
south direction, and has eut through the Tar Springs sand- 
stone, exposing the underlying Glen Dean and Hardinsburg 
formations in the bottom of the valley, but the hills on either 
side are of Tar Springs sandstone. Other outcrops of the for- 
mation are present in several fault blocks north of Princeton, 
between faults 3 and 28. In this area, east of the Princeton- 
Farmersville road, much of the higher land is underlain by the 
Tar Springs sandstone, and in some of the smaller blocks the 
sandstone has been dropped to the level of the creek valley 
floor. 

For a distance of about two miles northwest from the 
Princeton-Farmersville road, along the north side of fault 
No. 3, there is a narrow belt of Tar Springs sandstone in which 
the strata are dipping steeply to the northeast. Steeply dipping 
beds of the formation are also present along the northeastern 
border of the elongate, tilted block between faults 3 and 9. 
In a continuation of this same belt to the northwest, between 
faults 3 and 8, a sandstone formation alone has been observed | 
which is believed to be the Tar Springs. 

The only other area within the limits of the quadrangle 
which is underlain by the Tar Springs sandstone, is a narrow’ 
belt south of fault No. 1, extending westward from Flat Rock’ 
to the western border of the quadrangle. 

Iithologic characters. The Tar Springs formation includes’ 
a number of more or less massive sandstone ledges which are 
separated by arenaceous shales, with one horizon of carbonace- 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 69 





ous beds which becomes an impure coal in places. The best exhi- 
bition of the lower portion of the formation, about 76 feet, 
has been seen in the section at Walche’s cut. At the base is a 
massive sandstone ledge 31 feet thick. This sandstone is a 
persistent member of the formation throughout the extent of its 
outcrop in the quadranele. It is rather fine grained and light 
yellow in color, and in many localities in the quadrangle it is 
a distinet bluff making ledge, great masses of which have com- 
monly slumped down over the underlying shale beds of the 
underlying formations. In many places the position of the 
outerop of these earlier formations has been determined from 
the exposures of the massive basal bed of the Tar Springs. 

In Walche’s cut the massive basal bed of the Tar Springs 
is succeeded by a series of shaly beds, first 2 feet 8 inches of 
sandy shales, and then 15 feet 6 inches of black, carbonaceous 
-shales, at the top of which there is a small amount of very poor 
coal. The carbonaceous bed is followed by more massive yellow 
sandstone, rather evenly bedded in lavers 6 inches to 14 inches 
thick, the whole bed being 8 feet 7 inches thick. Above this 
there are 13 feet 3 inches of fissile shales, somewhat sandy in 
part, and this in turn is followed by 5 feet of thinly bedded 
vellow sandstone. This section does not constitute the entire 
thickness of the formatien, the remainder of it being cut. off 
by a fault which crosses the cut, the dislocation bringing the 
next sueceeding formation, the Vienna limestone, against the 
lower part of the Tar Springs. 

The higher portion of the Tar Springs sandstone is well 
exposed in some of the railroad cuts along the old line of the 
Illinois Central Railroad southwest of Claxton. Yn one of these 
cuts the formation can be seen passing beneath the Vienna 
limestone. The section at this place is an alternation of at least 
three rather massive ledges of fine-grained, vellow sandstone, 
the thickest one also the lowest one, being 20 feet 8 inches thick. 
The higher of the three beds is 4 feet 6 inches thick. Between 
the sandstone ledges there are thick beds of yellowish, thinly 
laminated, more or less sandy shales, the thickest bed being 
over 70 feet thick. The lowest beds in the section southwest 
of Claxton seem to be higher in position than the highest bed in 
Waleche’s cut. 


70 PRINCETON QUADRANGLE 





The outstanding features of the formation as a whole is 
the suecession of several massive sandstone ledges separated 
by more or less arenaceous shale members, with a carbonaceous 
or impure coal band some distance beneath the middle of the 
formation. The basal sandstone is the thickest and most mas- 
sive, and in most places where it outcrops it is a bluff forming 
bed. 

Tn his Chester section east of Princeton, Ulrich.2* has con- 
sidered the Tar Springs sandstone beds exposed in the railroad 
cuts southwest of Claxton on the old line of the Illinois Central 
Railroad, as Cypress, and his published description of the 
Cypress is in the main a description of the Tar Springs. 

Thickness. The complete thickness of the Tar Springs 
sandstone has nowhere been observed in one seetion in the 
Princeton quadrangle. In Walche’s cut there are 76 feet of 
the lower portion of the formation exhibited, and in the cuts 
southwest of Claxton there are 120 feet 8 inches of the higher 
part, and it is believed that there is no overlapping of the two 
sections, which would give a thickness of at least 198 feet 8 
inches, with the possibility of some additional beds not repre- 
sented in either section. A thickness of perhaps 200 feet may 
be assumed as the minimum for the formation. 

In the high hill/south of faulj<No. 31; and justeasmos 
Lamb’s Creek, the Tar Springs formation must occupy 120 
feet or more of the total height, this being the iower portion 
of the formation resting upon the Glen Dean limestone. <At 
the base the massive, bluff forming sandstone ledge is well 
exposed, but the higher strata are much talus covered. 
| Stratigraphic relations. The abrupt introduction of the 
massive sandstone beds of the Tar Springs, alone with the 
apparent variation in thickness of the underlying Glen Dean, 
this variation being in the upper beds of the formation, sug- 
vests the possibility of a relation of unconformity between the 
two formations. 

In the higher portion of the Tar Springs formation the 
sandstone membe>5 become thinner and the shale beds more 
ecnspicuous, and although the actual transition into the over- 


2a Ky. Geol. Surv., Miss. Foss. West. Ky.; pp. 74-75. 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 71 


lying Vienna limestone has not been observed, it is not improb- 
able that the passage is accomplished with no break in the 
sedimentation, and consequently with no unconformity. 

Paleontology. No fossils other than the fragmentary plant 
remains have been observed anywhere in the Tar Springs forma- 
tion in the Princeton quadrangle. 

Correlation. The correlation of the Tar Springs sandstone 
in the Prineeton quadrangle is based primarily upon its strati- 
eraphic position above the Glen Dean limestone, which is char- 
acterized by its peculiar assemblage of fossil species. A char- 
acteristic of some significance, however, may be the impure 
eoal bed which is present in the Tar Springs exposure in Wal- 
che’s cut. A similar coal bed has been recognized in the forma- 
tion at a number of localities in western Kentucky and southern 
Illinois, and seems to be a very persistent feature of the forma- 
tion. It 1s not possible to determine whether this Tar Springs 
coal bed was deposited contemporaneously throughout the whole 
southern Illinois and Kentucky section, but it is possible that 
such was the ease. 


VIENNA LIMESTONE 

Name. This formation was named from Vienna, Johnson 
County, Illinois, and it has been recognized as a persistent unit 
in the Chester section over much of southern Illinois and in 
western Kentucky. 

Distribution. In the Princeton quadrangle the Vienna 
limestone outcrops only to the northeast of the main line of 
faulting which crosses the area. Perhaps the best exposure in 
the district is in Walche’s cut, where the formation is faulted 
against the lower portion of the Tar Springs sandstone. An 
exposure may be seen in one of the vallevs between cuts on the 
old main line of the Illinois Central Railroad, southwest of 
Claxton, where it overlies the Tar Springs sandstone in its 
normal position. The formation is well exposed at Lewistown, 
also north and south of that place at a number of localities, just 
above the Tar Springs.. In*the northwestern part of the quad- 
rangle the characteristic chert beds of the for.aation are exposed 
at a number of localities about Farmersville, where the Vienna 
seems to be the lowest exposed formation. It is again exposed 


72 PRINCETON QUADRANGLE 





at a number of points adjacent to the upper boundary of the 
steeply dipping Tar Springs sandstone belt along fault No. 3, 
west of the Princeton Farmersville road. Other exposures may 
be seen in the vicinity of Flat Rock, where the upper boundary 
of the Tar Springs is present. 

Lithologic characters. The Vienna has two distinct mem- 
bers which seem to be present wherever the formation comes to 
the surface in the Princeton quadrangle, these being a highly 
cherty limestone below and a shale above. The position of out- 
crop of the lower member of the formation is commonly estab- 
lished by the presence of the residual chert which oceurs in 
abundance along with the residual clay of the formation. Such 
residual cherts are conspicuously present along the public high- 
ways wherever the roads cross the formation, along streams and 
in fields. The actual exposures of the limestone with the inclosed 
cherts are less commonly met with, but where it has been seen 
the limestone is gray in color, and more or less massive and 
compact in texture, or suberystalline. 





THE TRUNCATING EFFECTS OF EROSION. 


Weathered Vienna Limestone, Walche’s Cut, Illinois Central Railroad, 
east of Scottsburg. 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 73 





The chert commonly occurs in more or less continuous 
layers from one to three inches in thickness, which break up 
on weathering into subcubical fragments with dimensions equal 
to the thickness of the layer from which they come. In places 
the limestone itself is highly siliceous, and upon weathering the 
‘lime is leached out, leaving a porous, siliceous rock, yellow in 
color. The lithologic character of such leached beds is identical 
with similar beds of the same formation which are found so 
characteristically in the Vienna limestone in Johnson and Union 
Counties, Illinois. The similarity in this lithologie character 
of the formation in such widely separated localities is really 
remarkable. One excellent exposure of the formation in the 
south side of Walche’s eut gives a good exhibition of interbed- 
ding of the characteristic leached limestone and chert bands. 

The shales which constitute the upper portion of the forma- 
tion are rather thinly laminated and fissile in character, argil- 
laceous and free from sand, and dark blue or almost black, to 
eray in color. 

Thickness. The best section in the Princeton quadrangle 
from-which to determine the thickness of the Vienna limestone 
is that in Walche’s cut, where 54 feet of strata are referable 
to it, both the lower more calcareous beds and the higher shaly 
beds being well exposed. At no other locality in the quadrangle 
can the lower and upper limits of the formation be determined 
with any degree of accuracy, but the thickness of the formation 
probably remains rather constantly at about 50 feet. 

Stratigraphic relations. There is no reason to conelude 
that the Vienna is not in conformable contact with the forma 
tions both below and above it. Its actual contact with the Tar 
Springs sandstone has not been observed in the quadrangle, 
although the exposure in Walche’s cut is believed to extend 
essentially to the base of the formation. It is known that the 
Tar Springs becomes more shaly in its upper portion, and it is 
more than likely that the transition to the Vienna takes place 
without any break. The transition from the Vienna to the 
overlying Waltersburg is well shown in the Walche’s cut section, 
and there clearly was no interruption in the sedimentation in 
passing from the lower to the higher formation. 


74 PRINCETON QUADRANGLE 








Paleontology. The calcareous beds of the Vienna and some 
of the thinner layers of shales interbedded with them are more 
or less fossiliferous. The fossils, however, are commonly frag- 
mentary and consist largely of bryozoans of the more usual 
Chester types. No complete collections have been made from the 
formation. 


Correlation. The correlation of the Vienna formation in 
the Princeton quadrangle has been based essentially upon its 
stratigraphic position, and upon its peculiar lithologie char- 
acter, and in the absence of opportunity for the detailed study 
of fossil collections from the formation, these features seem to 
be sufficient evidence to establish the identity of the formation 
with the typical Vienna of southern I]linois. 


W ALTERSBURG SANDSTONE 


Name. The Waltersburg sandstone was first named from 
exposures in Pope County, [llinois. The formation has been 
found to be a persistent one across southern [llinois from the 
western part of Hardin, to Union County. The formation has 
been recognized in one loeality in Livingston County, Kentucky, 
and is now found to be more widely distributed and quite 
typical, in the Princeton quadrangle. 


Distribution. This formation has been found to be ¢o-ex- 
tensive with the underlying Vienna limestone in the Princeton 
quadrangle. Wherever the cherty Vienna limestone is present, 
there is some evidence of a thin sandstone formation overlying 
it, Separated by a thin shale interval, which is the Waltersburg. 


Lithologic characters. The Waltersburg varies somewhat 
in its characteristics from place to place, within the Princeton 
quadrangle, and in some places, as Walche’s cut, it contains a 
eonsiderable proportion of shale. Where the greater amount of 
shale is present in the formation, the sandstone is in thin beds 
distinetly jointed in two directions, one set of joints being close 
together, commonly three inches or less, and the other set 12 
to 20 inches apart. Jointing of this sort causes the beds, which 
are only two or three inches thick, to break up into elongate, 
splinter-like fragments which are very characteristic of the 
formation. In situations where these splintery beds have not 


~] 
{ 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 





been subjected to weathering, as in Walche’s cut, the sand- 
stone is dark in color upon freshly fractured surfaces, the 
outer surfaces of the beds being reddish brown. In more weath- 
ered situations the sandstone has been subjected to leaching and 
is yellowish in color. In many places where the public high- 
ways in the quadrangle have crossed the Waltersburg forma- 
tion, these fragments of sandstone, like sticks of stovewood, are 
conspicuous across the outerop. 

In some places the Waltersburg is more completely sand- 
stone in composition, in which case the formation is thinly 
bedded and commonly rather pale yellow in color. Even in 
exposures of this sort there is a tendency towards the develop- 
ment of the splinter-like fragments where the beds are broken 
up, but this type of jointing is less perfectly developed. 

The type of jointing, and the consequent form of the 
residual sandstone fragments of the Waltersburg, which has 
been described in the foregoing paragraphs, is not limited to the 
formation in the Princeton quadrangle, but occurs also in the 
same formation as far away as Pope and Johnson Counties, 
Illincis. It is really remarkable that such a peculiar char- 
acteristic of the formation should be so persistent over so great 
an area. Where the formation has its greatest development, 
near the line between Pope and Johnson Counties, Illinois, it 
is a massive, bluff forming sandstone 60 or more feet thick. 
This expression of the formation, however, is very limited in 
an east-west direction along the outcrop, and where it is traced 
to the east and to the west, it changes in a short distance into 
thin, splintery sandstone layers entirely like the beds in the 
Princeton quadranele. 

Thickness. The Waltersbure is one of the thinner forma- 
tions of the Chester Series in the Princeton quadranele, in the 
Walche’s cut section there being only 6 feet 8 inches of beds 
which can be referred to it. At this locality there are two 
splintery sand beds such as have been described, each 1 foot 4 
inches thick, separated by four feet of black shale. Where the 
formation is more completely sandstone it is somewhat thicker, 
but probably nowhere does it exceed 15 or 20 feet. 

Stratigraphic relations. From the evidence afforded by the 
fully exposed section in Walche’s cut, there seems to be no 


76 PRINCETON QUADRANGLE 








reason for recognizing any interruption in sedimentation either 
below or above the Waltersbure sandstone. 

Paleontology. No fossils have been observed in the Wal- 
tersburg, although it is not at all unlikely that some imperfect 
plant remains may occur in the formation in places. 

Correlation. The basis for correlating these beds in the 
Princeton quadrangle with the Waltersburg formation of Pope 
and Johnson Counties, Illinois, is its identical stratigraphic 
position, as determined especially by the overlying, highly fos- 
siliferous Menard limestone, and by the remarkable similarity 
in lithologic characters of certain exposures of the formation in 
the two regions. 


MeNaARD LIMESTONE 


Name. The Menard limestone was named from Randolph 
County, Illinois, where the formation is well exposed in the 
Mississippi River bluffs at Menard. The formation has been 
mapped across southern I!linois and into Kentucky. It is one 
of the more important of the Chester limestone formations, 
and is persistent in its lithologic and faunal characteristics. 

Mstribution. The Menard limestone is exposed in a num- 
ber of the fault blocks south of Claxton, and also occupies a 
considerable area northeast and south of Lewistown, between 
faults 31 and 53. A smaller area, continuous with the last 
mentioned on one side, and with the larger of the blocks south 
of Claxton on the other, is present in the fault block bounded 
by faults 50, 55, 56, 45, and 54. By far the largest outcropping 
area of the formation is in the northwestern portion of the 
quadrangle, between faults 1, 2, and 3. Jixcellent exposures 
of the formation can be seen in all directions from Farmers- 
ville, on the east to Big Cany Creek on the north and south to 
the faults, and on the west to the border of the quadrangle. 

lithologic characters. The lower portion of the Menard 
formation contains a considerable amount of shale interbedded 
with the limestone beds, which vary in thickness from a few 
inches to a foot or more. This portion of the formation is rarely 
well exposed in natural outcrops, because of its lithologic 
character, it being more or less completely talus covered, or is 
covered with residuum. The only locality where the basal part 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES ee 








of the formation is well exposed is in Walche’s cut. Some of 
these lower beds are abundantly fossiliferous, and in places the 
fossils have been silicified and occur in well preserved condition. 
in some of the residual clays. 

The higher portion of the formation is made up of more 
massive limestone beds, but these beds are commonly separated 
by shale partines from a few inches to several feet thick, the 
limestone ledges themselves varying in thickness up to 10 feet 
or more. The limestone is for the most part gray in color, and 
on weathering it commonly has smooth surfaces. The texture of 
the rock is in most places compact and little or not at all erys- 
talline, it is hard and brittle, and breaks with a splintery frae- 
ture. Some beds are darker colored than others, and more’ 
compact, but on the whole there is a notable similarity 
throughout. 

In some parts of the quadrangle there is apparently a thin 
sandstone member near the upper part of the formation, but 
in much of the area of outcrop such a member seems to be 
lacking. ) 

Thickness. In Walche’s cut the lower shaly portion of the 
Menard is approximately 30 feet thick, but the thickness of the 
remaining beds is not certainly determinable. In the north- 
western part of the quadrangle, however, at a number of places, 
there is an interval of 120 feet which must be occupied by the 
Menard limestone, and the whole formation may have a maxi- 
mum thickness of 140 feet within the quadrangle. 

Stratigraphic relations. There seems to be no interruption 
in the accumulation of sediments in passing from the underlying 
Waltersbure sandstone into the Menard limestone. At the top 
of the formation, however, there may be an unconformity. This 
condition is suggested by the abrupt change from limestone to 
sandstone sediments, and there seems to be some variation in 
the thickness of the Menard, which may be due to erosion pre- 
ceeding the deposition of the overlying Palestine sandstone. 
At some localities in southern [linois there is an undoubted 
unconformity at this horizon, and it is quite likely that the 
condition persists into Kentucky. 

Paleontology. The fossils of the Menard limestone are most 
abundant and best preserved in the lower part of the formation, 


78 PRINCETON QUADRANGLE 











in the more shaly beds. In the more dense limestone beds of 
the higher portion of the formation, the fossils are commonly 
so firmly imbedded that they are not easily collected or identi- 
fied, and they are also much less numerous than in the lower 
beds. A characteristic fauna from the lower Menard has been 
collected from the exposures in Walche’s cut, and the follow- 
ing species have been recognized : 


Menard Fauna from Walche’s Cut 


Triplophyllum spinuiosum (M.-E. & H.). 
Pentremites fohsi Ulrich. 
Pentremites sp. ; 

Pentremites sp. 

Agassizocrinus sp. 

Pterotocrinus menardensis Weller. 
Archaeocidaris sp. (spine). 
Fistulipora excelens Ulrich. 
Stenopora cestriensis Ulrich. 
Stenopora tuberculata Prout. 
Anisotrypa solida Ulrich. 

Fenestella cf. multispinosa Ulrich. 
Archimedes distans Ulrich. 
Archimedes intermedius Ulrich. 
Archimedes cf. swallovanus Hall. 
Polypora corticosa Ulrich. 

Orthotetes kaskaskiensis (McChesney). 
Productus ovatus Hall. 
Diaphragmus elegans (N. & P.). 
Spiriferina transversa (McChesney). 
Spiriferina spinosa (N. & P.). 
Spirifer increbescens Hall. 
Cliothyridina sublameiiosa (Hall). 
Composita subquadrata (Hall). 
Allorisma ciavata McChesney. 
Conularia sp. 


The larger number of the species mentioned in the above 
list are more or less widely distributed through the Chester 
faunas, but the large forms of Spirifer increbescens and Com- 
posita subquadrata are characteristic of the higher Chester 
faunas, and Pentremites fohsi and Pterotocrinus menardensis 
are limited to the Menard, so far as known, and are the most 
diagnostic species for this lower part of the formation. 





STRATIGRAPHIC GEOLOGY—CHESTER SERIES 79 





A number of other collections from the Menard limestone 
have been made in the quadrangle, all of them containing the 
usual species found in the formation, Spirifer increbescens and 
Composita subquadrata generally being the most common mem- 
bers of the faunas. The species Sulcatopinna nussouriensis, 
which is a common Menard species in much of southern Illinois, 
has been collected from a number of places, but the species has 
not been observed to be so common here ‘as it is 1n some other 
areas. 


Correlation. The correlation of. the Menard in the Prince- 
ton quadrangle is fully established by the presence of the fauna 
characterized by Pentremites fohst and Pterotocrinus menar- 
densis, Which are good zonal fossils for the lower Menard, being’ 
characteristic of this horizon across southern Illinois and else- 
where in Kentucky, and being unknown from any other posi- 
tion. Alone with the faunal evidence which is so conclusive, 
the lithologie similarity of the formation with the Menard else- 
where in western Kentucky and southern Illinois, gives addi- 
tional strength to the correlation of these beds in the Princeton 
quadranele. 


PALESTINE SANDSTONE 


Name. The name Palestine has been used widely in south- 
ern Illinois and western Kentucky for one of the higher sand- 
stones of the Chester Series. It was named from a_ locality 
in Randolph County, Illinois, where the typical exposures are 
to be found. It is the first one of the Chester sandstones which 
is developed uniformly across southern Illinois from the Ohio 
to the Mississippi Rivers, and the studies in western Kentucky 
have shown that it continues with similar uniformity at least as 
far as the Princeton quadrangle. 


Distribution. Most of the Palestine sandstone in the 
Princeton quadrangle is present within a belt crossing the area 
in a northwest-southeast direction, from the eastern border near 
Claxton to the northern border two miles east of Flat Rock. 
Outside of this belt the formation occurs southwest and west 
of Farmersville, capping a number of hills near fault No. 3. 
Within the diagonal belt above mentioned the sandstone does 
not oceur as a continuous outcrop. South of Claxton there are 


80 PRINCETON QUADRANGLE 





two smal areas of outcrop in two separate fault blocks, but 
aside from these all the outcrops occur in two of the larger 
fault blocks, one between faults 56 and 338, the other between 
faults 6 and 1. These two areas are separated by the down- 
dropped block of Pottsville between faults 33 and 6. The more 
extensive outcrop of the formation is present in the block be- 
tween faults 6 and 1, where its greatest width is nearly three 
miles towards the south border of the fault block. North of 
Briarfield Church the Palestine caps the hills west of Big 
Cany Creek, and northwest of Rufus the outcrop becomes more 
extended northeast of the same creek. A number of hills north 
of Farmersville, towards Big Cany Creek, are capped by isolated 
outerops of the formation, and other hills east, southwest and 
west of Farmersville are similarly capped by the formation. 
The largest of these hill-eapping outerops is situated north of 
Good Spring School. 
Inthologic characters. In general the Palestine isa brown 
to vellow sandstone, in places with a eeu tint, a 
texture it is rather fine and uniform. Tt is e up of more or 
less massive beds in parts of the formation, elsewhere it is thinly 
bedded, in places almost shaly in character. It is not notably 
different from the other more massive beds of sandstone in the 
Chester Series of the region, and exhibits no lithologic char- 
acter which would serve to identify it with certainty in situa- 
tions whete its stratigraphic position relative to the limestones 
of ee eould not be determined. 
Thickness. Where its full thickness can be best determined, 
1e Palestine sandstone seems to be approximately 60 feet thick. 


ee There are localities where the formation does not seem to be 


ve 


over 40 feet in thickness, the thinest exhibition of it being east 
of Big Cany Creek, southeast of Rufus. / 

Stratigraphic relations. The possibility of an unconformity 
between the underlying Menard limestone and the Palestine 
sandstone has already been mentioned. At the top of the forma- 
tion there is no evidence exhibited within the quadrangle, ,so 
far as observations have been carried, to either establish or dis- 
prove the presence of a stratigraphic break between it and the 
overlying limestone. Throughout western Kentucky and south- 


STRATIGRAPHIC GHOLOGY—CHESTER SERIES 81 











ern Illinois this horizon is generally obscure, but at a few local- 
ities it seems to be clear that there was no interruption in sedi- 
mentation at this horizon, and it is quite likely that this is the 
condition throughout. 

In the east central portion of the quadrangle, at two local- 
ities, one a mile and one-half northeast of Claxton, the other 
a mile northwest of Lewistown, the higher beds of the Chester 
have been eroded before the deposition of the Pottsville sand- 
stone of the Pennsylvanian, so that the Pottsville rests uncon- 
formably upon the Palestine sandstone. 

Paleontology. As in other sandstones of the Chester Series, 
the only fossils which are likely to be met with in the Palestine, 
are fragmentary plant remains, broken trunks of a species of 
Lepidodendron being the most common. Even these fossils have 
not been observed in the Princeton quadrangle, although they 
may well be present somewhere, and are likely to be met with 

A _if-farther search is made. With our present knowledge even 
the plant remains, if they should be found, would serve to be 
of little value for purposes of correlation, for the same things 
seem to occur in the several sandstones of the series. 

Correlation. The correlation of the Palestine sandstone 
in the Princeton quadrangle is dependent wholly upon its strati- 
eraphic position between the Menard and Clore limestones. <A 
similar sandstone occupies this position throughout western Ken- 
tucky and southern Illinois, and it is undoubtedly a continuous 
bed spreading from western Kentucky to Randolph County, 
Illinois. 

CLORE LIMESTONE 


Name. The Clore limestone is another formation which 
was originally named in Randolph County, Illinois. It has been 
traced across southern Illinois and western Kentucky as far 
as the Princeton quadrangle. 

Distribution. The Clore limestone occupies a narrow belt 
of outcrop, overlying the Palestine sandstone, extending from 
near Claxton in a northwest direction to the northern border of 
the quadrangle about six miles east of the northeast corner. 
Another similar outcropping belt, about one and one-half miles 
in length, also having a northwest-southeast direction, lies a 
little west of Bethany School. 


e 





82 PRINCETON QUADRANGLE 








Throughout its whole extent the Clore is commonly rather 
poorly exposed, being so situated that it is likely to be more or 
less covered with talus from the overlying beds. Along a por- 
tion of the main belt of outcrop of the formation, for a short 
distance northwest of Claxton, and again northeast of Lewis- 
town, the Clore formation, along with all the higher beds of the 
Chester series, have been eroded before or during early Penn- 
sylvanian time, so that the Pottsville formation rests upon the 
underlying Palestine sandstone. . 

Lithologic characters. The Clore formation consists of 
interbedded limestone and shale. The relative proportion of the 
two types of sediments is not easily determined because of the 
usual talus covering which obscures the formation in most places, 
but there is probably more shale than limestone. The limestone 
is more or less variable in character, but the beds most com- 
monly exposed are in general light to dark gray in color, hard 
and more or less brittle, and compact in texture. The beds 
weather with smooth surfaces, which are likely to be somewhat 
lighter colored than the freshly broken surfaces. The limestone 
beds of the Clore are not unlike similar beds which occur in the 
Menard limestone below, or in the Kinkaid limestone which 
occupies a still higher position. 

Thickness. It is somewhat difficult to determine with any 
accuracy, the thickness of the Clore formation in the Princeton 
quadrangle. Perhaps the most satisfactory localities to estimate 
this thickness are along that portion of the outcrop extending 
northwest and southeast from Peach. In this district there is 
an interval above the Palestine sandstone as great as 60 feet 
which may be occupied by the Clore. This amount would be the 
maximum, and in all probability the actual thickness is some- 
what less. Elsewhere in the quadrangle there seems to be less 
room for the formation, where it may be only 30 to 40 feet 
thick. Throughout the whole extent of the formation, from the 
Mississippi River sections in Illinois, to that portion of Ken- 
tucky covered in this report, the thickness of the Clore forma- 
tion varies from 30 to 60 feet, about 40 to 50 feet being the 
more usual thickness, so that the thickness of the formation in 
the Princeton quadrangle agrees very well with that exhibited 
elsewhere. 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 3 





Stratigraphic relations. Continuous exposures of this por- 
tion of the Chester Series are not met with in the Princeton 
quadrangle, so that little can be determined regarding the strati- 
eraphie relations of the Clore formation, either with the under- 
lying Palestine or with the overlying Degonia sandstone. No- 
where in southern Illinois or in Kentucky have any facts been 
observed in connection with the formation to establish relations 
of uneonformity between it and either the underlying or over- 
lying sandstones, and in all probability the sedimentary sue- 
cession is unbroken at both of these horizons. 

Paleontology. Throughout the extent of the Clore lme- 
stone in southern Illinois and western Kentucky, the presence 
of delicate cylindrical bryozoans belonging to the genus Batosto- 
mella, have been observed very generally in some portion of the 
formation. The species commonly met with is B. nitidula, and 
although this and perhaps other similar Clore species are present 
elsewhere in the Chester Series, they seem to be most abundant 
in some beds of the Clore. Another species which to the present 
‘time has only been observed in the Clore formation, is a large 
species of Productus, probably undescribed. In the Princeton 
quadrangle the large Productus has not been observed, but the 
common presence of examples of Batostomella has been met 
with in at least one locality near the southwestern corner of the 
Tradewater rectangle. Systematic search for a good collection 
of the Clore fossils has not been made, however, and it is not 
unlikely that representative collections may be secured at some 
future time. ) 

Correlation. So far as any paleontological evidence has 
been secured, it substantiates the correlation of this unit in the 
Princeton quadrangle with the Clore throughout western Ken- 
tucky and southern Illinois, but such evidence, so far as it has 
been gathered to date is insufficient. The position of this strati- 
oraphie unit in the regular Chester sequence, however, its thick- 
ness and general lithologic character, seem to fully warrant the 
reference of the bed to the Clore formation. 


DEGONIA SANDSTONE 


Name. The Degonia sandstone was named from Jackson 
County, Illinois, where the formation is an important. cliff 


84 PRINCETON QUADRANGLE 








forming member of the Chester Series in the Mississippi River 
bluffs. The formation has been recognized and mapped across 
southern Illinois and also in the adjacent portion of western 
Kentucky, and is now known to extend at least as far east as 
the Princeton quadrangle. 

Distribution. The distribution of the Degonia sandstone 
in the Princeton quadrangle follows closely that of the under- 
lving Clore limestone. In most parts of the area it is a narrow 
belt because of the limited thickness of the formation. In many 
places the exposures are poor, but in most sections the residual 
blocks of sandstone very definitely mark the position of the out- 
crop. Perhaps the most extensive exposure of the formation is 
along the road leading north from Princeton to Liberty Sehool, 
where for nearly a mile north from Peach this sandstone is 
exhibited in numerous exposures. 

Iathologic characters. The Degonia is similar in character 
to much of the other sandstone of the Chester Series in the 
Princeton quadrangle, and it possesses no distinctive features 
by means of which it can be certainly recognized, apart from 
its stratigraphic position. It is fine grained, hght yellow to 
brownish in eolor, and rather thinly bedded. 

Thickness. The Degonia is one of the thinner sandstones 
in the Chester Series of the Princeton quadrangle. None of the 
outcrops are such that the whole of the formation ean be 
observed and measured direct, but in certain places the possible 
limits of the formation can be established with some degree of 
accuracy. Nowhere in the area does it seem to exceed 30 feet 
in thickness, and in places it is probably 20 feet or less. 

Stratigraphic relations. There are no data at hand to show 
that the Degonia sandstone in this region is unconformable with 
either the underlying or overlying formations. 

Paleontology. No fossils of any sort have been observed in 
this sandstone in the area under consideration, but it is not at 
all unlikely that more or less fragmentary remains of plants 
may be discovered in the formation. 

Correlation. The correlation of the Degonia sandstone in 
this part of Kentucky is based entirely upon its stratigraphic 





STRATIGRAPHIC GEOLOGY—CHESTER SERIES | 85 


-—« 








position between the Clore and Kinkaid limestones whose equiva- 
lence with the limestones of southern Illinois is established with 
certainty by their fossil contents. 


KINKAID LIMESTONE 

Name. The name of this limestone was derived from Kin- 
kaid Creek in Jackson County, Hlinois. It is one of the more 
important limestones of the Chester Series, and in much of its 
extent from the Mississippi River to western Kentucky it is 
the thickest limestone of the whole series. 

Distribution. In the Princeton quadrangle the greatest 
extent of the Kinkaid hmestone is present alone a belt extend- 
ing northwest from Claxton to about the middle of the north 
boundary of the quadrangle, this belt being interrupted for the 
distance of about one and one-half miles by the down-dropped 
block of Pottsville sandstone between faults 7 and 33. The 
next largest area of outcrop is in the extreme northwestern cor- 
ner of the quadrangle, north of fault No. 1, where the forma- 
tion occupies the floor and sides of the valleys, being overlain 
by the Pottsville. <A third area of outcrop is in the truncated, 
wedge-like block which is down-dropped between faults 5, 3, 
and 6, and adjacent to this on the south is a small area between 
faults 3 and 6, in the valley of a tributary of Phelps Creek, 
which is exposed by erosion of the overlying Pottsville. Far- 
ther to the east, along Phelps Creek, the Kinkaid is exposed in 
the elongate trapezoidal fault block bounded by faults 3, 24, 25, 
and 33. 

Along a part of the main belt of outcrop of the formation, 
extending northwest from Claxton, the pre-Pottsville erosion 
was sufficient to remove the entire thickness of the Kinkaid, as 
well as the underlying Degonia and Clore formations, so that 
the Pottsville sandstones rest upon the Palestine sandstone. 
Where the Pottsville rests upon formations older than the Kin- 
kaid there is of course an interruption in the continuity of the 
outcrop of the limestone, two such interruptions being present, 
the larger one a mile and one-half northwest of Claxton, and 
the smaller one a mile east of Lewistown. 

Iathologic characters. The Kinkaid formation is an alter- 
nating series of limestone and shale beds, varying in thickness 


&6 PRINCETON QUADRANGLE 








and in lithologic characters. The best exposures of the forma- 
tion are situated on more or less steeply sloping hillsides, and 
in ledges which border some of the streams which cross the belt 
of outcrop. The hillside outcrops are commonly represented by 
partially exposed ledges and by slumped masses of limestone, 
the actual exposures of shale beds being unusual. Because of 
the nature of the exposures and the amount of talus covering, 
it has not been possible to construct a detailed section of the 
whole formation. | 

The several limestone members of the formation differ more 
or less in character and thickness. In general they are very 
evenly bedded, in any one member the beds commonly being 
somewhat uniform in thickness, and being separated by shaly 
partings. Some of the limestones are light-gray in color, weath- 
ering with smooth surfaces, hard and compact in texture, break- 
ing with splintery fracture, not unlike much of the Menard 
limestone. Other beds are more argillaceous with more con- 
spicuous shaly partings between the individual layers. None 
of the beds observed are notably crystalline in character. The 
shale members are probably as variable in character as the 
limestones, but they are not so readily observed. Some beds 
are more or less calcareous, others are wholly argillaceous, and 
they vary in color from black or nearly black to light gray. 
Some beds are quite fissile in character, others are more massive. 

In the lower portion of the formation there seems to be 
present in most or all sections, a thin sandstone member. In 
character this sandstone is not unlike other Chester sandstone 
beds, but the actual exposures are obscure, and it is commonly 
represented by more or less seattered residual blocks upon the 
hillsides. A similar sandstone member has been observed in 
the Livingston County, Kentucky, section. 

The Kinkaid section in the Princeton quadrangle differs 
notably from that of Livingston County, and much of southern 
Tllinois, in the absence of a conspicuous chert bed near the base 
of the formation, beneath the sandstone member. There is, 
however, a considerable amount of chert in places associated 
with the formation at its very summit. This chert bed has 
nowhere been observed in situ, it occurs in the form of loose, 
irregular masses upon the hill slopes at or just beneath the line 


STRATIGRAPHIC GEOLOGY—CHESTER SERIES 87 








of contact between the Kinkaid and the overlying Pottsville, 
and it is not improbable that they were originally masses of 
residual chert upon the pre-Pennsylvanian land surface. This 
chert horizon is by no means so conspicuous as that in the lower 
part of the formation farther west, nor is it so conspicuous a 
chert zone as the Vienna limestone within the Princeton 
quadrangle. 

Thickness. In view of the fact that the pre-Pennsylvanian 
erosion has in places removed the entire Kinkaid formation, and 
the underlying Degonia and Clore, the actual thickness 
of the formation in the Princeton quadrangle varies from zero 
to the maximum amount present, which may be as much as 100 
feet. This thickness is not as great as in some localities farther 
west, in Kentucky and Illinois, where as great a thickness as 
180 feet or even 200 feet is known in certain sections. 

Stratigraphic relations. The stratigraphic relations be- 
tween the Kinkaid limestone and the underlying Degonia sand- 
stone have already been considered. At the summit of the for- 
mation there is everywhere a great unconfcrmity between the 
Chester Series and the Pennsylvanian. 

Paleontology. In many places the limestones of the Kin- 
kaid formation are not conspicuously fossiliferous. Where fos- 
sils are present they are for the most part brachiopods of the 
usual Chester types, great numbers of individuals of Composita 
and Spirifer being present in some localities, with lesser num- 
bers of other genera of brachiopods, and some molluses. The 
bryozoans are much less conspicuous in the Kinkaid than in 
other Chester limestones, although some of the usual Chester 
genera such as Archimedes, etc., are locally present. Crinoidal 
remains are also less commonly present than in most of the 
other limestones of the series. 

A characteristic Kinkaid fauna from a locality three- 
fourths of a mile west of Claxton contains the following species : 


Fauna of the Kinkaid Limestone Near Claxton 


Triplophyllum spinulosum (M.-E. & H.). 
Fenestella sp. 

Polypora approximata Ulrich. 
Orthotetes kaskaskiensis McChesney. 
Diaphragmus elegans (N. & P.) 


88 PRINCETON QUADRANGLE 








Camarophoria explanata (McChesney). 
Girtyella indianensis (Girty). 
Girtyella brevilobata (Swallow). 
Spirifer increbescens Hall. 
Humetria vera (Hall). 
Cliothyridina sublamellosa (Hall). 
Composita subquadrata (Hall). 
Aviculopecten sp. 

Modiola sp. 

Bellerophon sp. 

Straparollus sp. 

Phillipsia sp. 


Correlation. The correlation of the Kinkaid is simply a 
matter of tracing the outcrop of the formation from place to 
place across western Kentucky and southern Illinois. The out- 
crop is discontinuous because of the extensive faulting, but the . 
position of the limestone immediately beneath the Pennsyl- 
vanian sandstones, and its similar lithologic and faunal char- 
acters, renders its recognition and correlation certain. 


CHAPTER V. 


STRATIGRAPHIC GEOLOGY, PENNSYLVANIAN 
SYSTEM 


CASEYVILLE FORMATION 


Introductory statement. All the strata of Pennsylvanian 
age which are exposed in the Princeton quadrangle are of Potts- 
ville age, and so far as they have been examined in detail they 
belong to the Caseyville formation, although some representation 
of the Tradewater formation may be present in the extreme 
northeastern part of the area. No attempt has been made in 
the prosecution of the present work to make a complete examl- 
nation of the Pennsylvanian area, the observations being limited 
to the establishment of the boundary between the Chester Series 
below and the overlying beds. 

Name. The name Caseyville formation was applied to the 
lowest division of the Pottsville rocks as they are represented in 
this portion of western Kentucky by Glenn, from the town of 
Caseyville! in Union County, Kentucky. The name has since 
been adopted for the equivalent strata in southeastern Ilinois, 
and will probably be applicable entirely across southern Illinois. 

Lithologic character. The lithologie characters of the 
Caseyville are similar throughout the extent of the formation, 
there being several massive sandstone beds separated by thinly 
bedded, shaly sandstone, with more or less clay shale. The more 
massive beds stand out in many places as prominent bluffs, but 
the sotter, less resistant beds are commonly more or less com- 
pletely covered by talus accumulation. 

In many places the more massive sandstone members of 
the formation are characterized by the presence of great numbers 
of rounded, white guartz pebbles, constituting veritable con- 
elomerate layers, the pebbles varying in size from one-eighth of 
an inch to nearly an inch in diameter. The amount of the con- 
olomerate varies greatly from place to place within the forma- 
tion, but even where the quartz pebbles are lacking entirely, the 
Pottsville sandstone cannot be easily mistaken for any of the 


1Coal of. the Tradewater River Region, Ky. Geol. Surv., Bull. No. 17. 


90 PRINCETON QUADRANGLE 


Chester sandstones, because of its coarser texture. The most 
conspicuous conglomerate beds seems to be present where the 
pre-Pottsville unconformity is the greatest, as in the region 
about Claxton. 


Coal. No extensive coal mining has been attempted at any 
locality in the Princeton quadrangle. Thin coal seams are pres- 
ent locally and in a few places have been worked a little for local 
consumption, 


Distribution. The greater portion of the Pottsville rocks 
in the Princeton quadrangle is confined to the northeastern por- 
tion of the area. The boundary of the formation starts near the 
middle of the northern boundary of the quadrangle, and con- 
tinues southeasterly in a sinuous line, interrupted in places by 
faulting, to the eastern border of the quadrangle east of Claxton. 

Besides this main area of Pottsville in the quadrangle, the 
formation is present in a number of the down-dropped fault 
blocks in different parts of the area. The largest of these blocks 
hes chiefly in the extreme northern portion of the Claxton and 
Princeton rectangles, and extends in a nearly east-west direction 
between faults 6, 7, 33, and 3, with a maximum width of over 
one mile in the northeastern part of the Princeton rectangle. 
Most of the other down-dropped blocks of Pottsville are present 
wholly or in part in the northren half of the Princeton rectangle. 
The larger one lies south of Phelps Creek, bounded by faults 
24, 25, 26, 28, and 17. In a narrow block about one and one- 
half miles in leneth, lying mainly between the two blocks already 
mentioned, and bounded by faults 24, 25, 38, and 3, the Pottsville 
caps the hills with the Kinkaid limestone exposed beneath. A 
small triangular block of Pottsville is present in the north- 
western part of the Princeton rectangle, bounded by faults 22, 
23, and 17. Two contiguous Pottsville blocks are present west 
and northwest of Princeton in the Princeton and Crider ree- 
tangles. These constitute some rough hills and are bounded 
by faults 33, 40, 41, and 42. Two other very small blocks have 
been recognized, one in the southwestern part of the Farmers- 
ville rectangle, bounded by faults 16, 17, 18, and 3, the second 
is in the Claxton rectangle, one-half mile southeast of Claxton, 
bounded by faults 58, 59, and 60. 


STRATIGRAPHIC GHOLOGY—PENNSYLVANIAN SYSTEM 91 











Thickness. No accurate determination of the thickness of 
the Caseyville formation within the Princeton quadrangle has 
been attempted, but it can be safely estimated as being 400 feet 
or more. 

Paleontology. No attempt has been made to collect the 
fossil plants from the Pottsville horizons in the Princeton quad- 
rangle, although in some localities well preserved impressions 
of Lepidodendron trunks have been observed in the sandstones. 

Correlation. Nothing new in regard to the correlation of 
the Pottsville of western Kentucky can be added from recent 
studies in the Princeton quadrangle. Floras from similar hori- 
zons elsewhere in this portion of the state and in southeastern 
Illinois, have been studied by David White, and his observations 
have led him to the conclusion that the Caseyville formation 
occupies a horizon near that of the Sharon conglomerate of 
western Pennsylvania. 





CHAPTER VI. 
STRATIGRAPHIC GEOLOGY, LAFAYETTE GRAVEL 


Nane. The youngest formation in the Princeton quad- 
rangle, aside from the recent, surficial materials, is a gravel 
deposit, largely unconsolidated in character, which caps some 
of the higher hills in the western and southwestern portions of 
the area. These deposits doubtless represent the widely dis- 
tributed formation to which the name Lafayette Gravel has 
been apphed, although it is generally believed at the present 
time that gravels of different age and origin have been included 
under this name. The name may be used temporarily at least, 
for the deposits in the Princeton quadrangle, until all of the 
widely distributed similar gravels have been more thoroughly 
studied and are better understood. 

Distribution. These gravel deposits occupy two distinct 
but strictly limited areas in the quadrangle at the present time. 
The first of these 1s west of Princeton, in the Crider rectangle, 
beginning on top of the ridge just east of White Sulphur 
Church, and capping the hills in a westerly and southwesterly 
direction for a distance of nearly four miles. The exact eleva- 
tion of the base of this gravel formation cannot be determined 
with certainty, for the pebbles have been washed far down the 
slopes and into the stream valleys, in some places for two or 
more miles from their source. At White Sulphur Church the 
original deposits seem to lie at an elevtion of about 600 feet 
above sea level, but along the same ridge to the east, where it 
rises to an elevation above 600 feet, the gravel is apparently 
lacking. Three miles southwest of White Sulphur the base of 
the formation seems to occupy an elevation of about 640 feet. 
These elevations can only be considered as approximate, but 
where the pebbles are associated with the angular, residual 
cherts of the underlying formations, they are considered as 
having been washed down from their original position. Pre- 
sumably the surface upon which the gravels were originally 
deposited was approximately a plane, and the differences in 
present elevation may be indicative of comparatively recent 
warping of the surface. 


94 PRINCETON QUADRANGLE 


The second area of outcrop of the gravels is in the Sara- 
toga rectangle, in the extreme southwestern corner of the quad- 
rangle, on the hills west and northwest of Friendship School. 
In this area the elevation of the original deposits seems to be 
near 580 feet, which is somewhat lower than in the area 
deseribed. Elsewhere in the quadranele there are hills with 
similar elevations to those mentioned, upon which no gravel 
deposits are present. | 

Inthologic character. These hilltop gravels are made up 
of smoothly rounded chert pebbles, varying in size up to a 
diameter of four or five inches. The cherts which are repre- 
sented in the deposits are various in character, but most of them 
are of such a nature as to suggest their origin from the St. 
Louis and Ste. Genevieve limestones of the immediate region. 
A small proportion of the pebbles, however, may have had a 
more remote origin. Most of the gravel seems to be wholly uncon- 
solidated, but in places it has been cemented into an iron econ- 
olomerate or in a sand conglomerate. Masses of these con- 
olomerates, some of them a foot or more in their dimensions, 
are common in the beds of ravines which head against the hills 
which are covered by the formation. In places the heads of 
these ravines are more or less completely filled in their beds, by 
a semi-cemented mass of these pebbles imbedded in red residual 
clay, which is more or less sandy in places. In most of such 
exposures there are a greater or less number of angular frag- 
ments of residual cherts from the underlying limestones, which 
suggest that these deposits are secondary from the original 
oravel accumulations. 

Origin. The smooth, rounded character of the pebbles in 
these hilltop gravels show that they must have been formed by 
running water or by wave action along a beach. Neither run- 
ning water nor wave action could place the pebbles in their 
present position upon the hilltops with the present topography. 
At the time when these gravel beds were laid down the present 
Princeton quadrangle, or at least some portion of it, must have 
been a part of a plane, the present hilltops oecupied by the 
gravel being remnants of this plane, the present topography 
of the area having been developed since the period of gravel 
accumulation. 


STRATIGRAPHIC GEOLOGY—LAFAYETTE GRAVEL 95 








Age. The age of the gravel formation is doubtless the 
same as that of other widely distributed hilltop gravels which 
are present in the Ohio and Mississippi Valleys. Although there 
may be some difference in the time of accumulation from place 
to place, the age of most of the gravel deposits doubtless falls 
within late Tertiary time, and they are commonly considered as 
having been formed during the Pliocene period. 





CHAPTER VII. 
IGNEOUS ROCKS 


Throughout the faulted region of western Kentucky and 
southeastern Illinois, a considerable number of igneous dikes 
have been observed. These dikes are commonly much weathered 
at the surface, and their residuum is commonly spoken of by the 
prospectors of the region as mica dirt. All of the dikes are 
basic in character, and those that have been studied petrograph- 
ically have been identified as Peridodite or Lamprophyre, and 
all of the others are of the same general character. When fresh 
the rock is mostly dark in color, nearly black or with a greenish 
tint, although in a few places a lghter colored rock has been 
observed. In texture the rock is mostly very dense and com- 
pact, some occurrences of it being characterized by the presence 
of considerable amounts of black mica in flakes up to one-fourth 
of an inch in diameter. The rock is extraordinarily tough, 
when fresh, and difficult to break with a hammer. When weath- 
ered these dike rocks are soft and friable, commonly somewhat 
olive green or vellowish in color, and they give rise to a brown- 
ish residual soil which differs from the residuum of any of the 
sedimentary rocks of the region. 

The origin of the dike rocks is totally different from that 
of the sedimentary rocks with which they are associated. Orig- 
inally they were in the condition of molten lava which was 
injected into these sedimentary rocks from below, under great 
pressure. They undoubtedly connect, somewhere far beneath 
the present surface, with a great intrusion of igneous matter 
which perhaps extends as far as the limits of distribution of the 
dikes themselves, or farther. It is not possible to determine 
the depth of such an intrusion, for it has nowhere been pene- 
trated by deep drilling or by mining operations, and is prob- 
ably many hundreds of feet beneath the present surface. 

Although the surface area occupied by the igneous rocks 
in western Kentucky ig infinitessimal as compared with the 
sedimentary rocks, their importance is great, since the primary 
factor in the accumulations of the great deposits of fluorspar in 
the district has perhaps been the presence of this igneous 
intrusion. 


98 PRINCETON QUADRANGLE 


Previously to the present field studies no dike rocks have 
ever been recorded from the Princeton quadrangle, the most 
numerous occurrences being in Crittenden County, but during 
the progress of the present work a dike has been discovered 
just west of the easternmost branch of Cany Creek, 1.1 miles 
southeast of Briarfield Church, and 1.5 miles north of Bethany 
Chureh. This dike is exposed in the heads of several short 
gullies. The exposure is not such as to permit the determination 
of its direction, but if the direction conforms with that of most 
of those in the district, it extends northwesterly and _ south- 
easterly. The rock itself is deeply weathered, and no fresh ma- 
terial whatever has been observed. In its present condition it 
is soft and friable and is just as easily eroded as the residual 
clays which are adjacent to it. The occurrence might not have 
been suspicioned except that the gullies were freshly cut when 
they were first visited. It is not improbable that numerous 
dikes may exist throughout this district which have never been 
observed because of their surficial covering, and for the same 
reason many of them may never be discovered. 


CHAPTER VIII. 
STRUCTURAL GEOLOGY 


In common with the region to the west and northwest of the 
Princeton quadrangle, extending to the Ohio River and con- 
tinuing beyond that stream into Illinois, the area included in 
this quadrangle is extensively faulted. This entire faulted dis- 
trict has an extent of 60 miles or more in an east-west direction, 
and over 50 miles in a north-south direction. The fault pattern 
throughout the whole area is remarkably complex, but scattered 
about locally there are small areas where the complexity of the 
faulting greatly exceeds that elsewhere. In the Princeton quad- 
rangle the most complex of these areas lies southwest of Claxton, 
although a belt of more than commonly complex faulting con- 
tinues northwestwardly across the quadrangle from the eastern 
border just south of Claxton to near the northwest corner. 

Throughout the entire general area which has been men- 
tioned the faulting is similar in character. The faults are in the 
main normal or tension faults, produced by the stretching of the 
earth’s crust, and it is important to consider the source of the 
forces which caused the stretching. Seattered about through 
the faulted area there are a number of igneous dikes exposed. 
The exposures of these dikes are perhaps most numerous in the 
Ohio River bluffs, although they may be actually no less num- 
erous elsewhere, the absence of surficial material upon the bluffs 
being responsible for their more common appearance. Where 
covered with the surficial materials the dikes are deeply weath- 
ered and are exposed only in a more or less accidental manner. 
During the summer of 1921 a previously unknown dike was dis- 
covered at a locality about five and one-half miles north of 
Princeton, in the head of a recently excavated gulley. This 
dike is much decomposed and its presence would never have 
been suspected except for the favorable location of the gully 
in which it is exposed. Doubtless there are scores of dikes 
throughout the faulted area which are completely hidden, and 
many of them may never be exposed to observation. 

The presence of these scattered dikes through the faulted 
region suggest the presence of a deep seated igneous intrusion 
of wide extent, underlying the whole area. Such an igneous 


100 PRINCETON QUADRANGLE . 





mass has never been penetrated by deep excavation or drilling, 
but its presence can probably be safely assumed, and its pres- 


ence may be considered as being responsible for the bowing up 


and consequent stretching of the crust which has resulted in the 
faulting of the region. The fracturing of the crust by the 
stretching consequent to the intrusion, broke the rock strata 
into more or less wedge-shaped masses, varying greatly in dimen- 
sion and form, some of them being only a few acres in extent, 
while others are square miles in area. All of the rock strata 
overlying the intruded mass must have been upraised by the 
lifting force of the intrusion, but the several wedge-shaped 
blocks produced by the fracturing of the strata slipped down- 


= ® ‘ : 


ward relative to each other in order to take up the slack pro- 


duced by the crustal stretching. In places the downcrowding 
of the wedge-shaped blocks has produced sufficient lateral pres- 
sure to occasion small thrust faults of very minor importance, 
such as the one exhibited in Walche’s cut, east of Scottsburg. 
Thrust faults of this character are of such small extent that they 
would never be detected except in a clean exposure such as is 
present in a fresh railroad eut or similar situation. 

Associated with this complex faulted area of western Ken- 
tucky and southeastern Illinois, are the famous fluorspar 
deposits of the region. The more important of these deposits 
are in the form of more or less vertical veins along the faults. 
Fluorine is known to be a product of igneous rocks, and the 
fluorine content of the mineral fluorite doubtless was derived 
in some manner from the igneous magma underlying the region. 
Locally there are horizontal fluorspar deposits of limited extent, 
apparently filling solution cavities in the Ste. Genevieve lime- 
stone, which are probably secondary in origin as compared with 
the fault vein deposits. 

The best exposure in the Princeton fr exhibiting 
the characteristic faulting of the area, is in Walche’s cut on the 
new line of the Illinois Central Railroad, between Scottsburg 
and Claxton a little more than one mile west of the last men- 


Sede, 


tioned station. The faulting is also well exhibited along the old: 
line of the same railroad, a mile or more southwest of Claxton. ' 
The accompanying graphic section of the strata exhibited in. 


Walche’s cut will serve to show the character of faulting in that 


a: 











Palestine 


Sandstone’ 








Menard 













Limestone 








WENTUCIXY GEOLOGICAL SURVEY 
SERIES VI 


WILLARD ROUSE JILLSCN 
DIRECTOR AND STATE GEOLOGIST 


1922 


Waltersburg 
Sandstone 











STRUCTURE SECTION 


5 
Watcne'’s Curt 
ILLINoIa CENTRAL RAILROAD 
East of ScottTsaurG 


by 
Stuort Weller 


FIG XII 


‘Cel 00Y OF THE PRINCETON, K¥%, QUADRANGLE” 
Scals, vactical and horizontal (ina 150 feat 





Mardiasburg 
 Sondstone 
Ee rarer 


if 


Golconda 
















= Renault Limestone s 








Bethel Sandstone 







So 
, Renault Limestone 








STRUCTURAL GEOLOGY . 101 
exposure, where practically every formation » & Chester 
Series present in the quadrangle may be seen. 

The amount and complexity of faulting in he Princeton 
quadrangle is evidenced by the fact that no less than 88 dis- 
tinet faults have been mapped within its boundaries, but the 


‘faults are not uniformly distributed through the entire quad- 


rangle. They are most numerous along a belt varying from 
one to three miles in width, extending across the quadrangle 
in a northwest direction from the eastern boundary south of the 
line of the Illinois Central Railroad, to the western border about 
half way between the line of the Evansville branch of the same 
railroad, and the northwestern corner of the quadrangle. 
Although the dominant direction of the faulting in this belt, 
established by the longer and. more continuous faults, is north- 
west-southeast, there are faults within the belt whose direction 
lies in all points of the:eomypass:. . ..-- ... -! 

Other faults in the quadrangle, especi ially across its south- 
ern third, are nearly east-west in direction, and there are a 
number of east-west faults entering from the east, or crossing 
the main northwest-southeast belt. A number of faults north- 
west of Princeton diverge from the main belt of faulting in a 
southwesterly direction, and a similar northeast-southwest fault 
erosses the northwestern corner of the quadrangle at Flat Rock. 
Other southwest-northeast faults are present southeast of Scotts- 
burg, connecting some of the more continuous east-west faults. 

This whole fault pattern is markedly different, so far as 
the direction of the faults is concerned, from that exhibited in 
the Cave in Rock and Golconda quadrangles, north and west of 
the Princeton quadrangle, and in the continuation of the faulted 
area into Illinois, where the dominant direction is northeast- 
southwest, the direction being more northerly than in the case 
of the northeast-southwest faults in the Princeton quadrangle. 

In addition to the many faults of the region, ‘a well de- 
fined dome has been recognized in the area between faults 1 and 
3, west of Farmersville. This Farmersville dome has been fully 
described in an earlier publication of the Survey. 

During the late summer and autumn of 1922 a well was 
drilled upon the Farmersville dome by the Atlas Oil Company, 


. -my. Geol, Surv., ser. 6, vol. 6, pp. 221-227 (1922). 





102 PRINCETON QUADRANGLE 





under the direction of their geologist, Mr. D. P. Hynes,” and 
the strata penetrated are as follows: 


Log of Well Three-fourths Mile West of Farmersville. 
Thickness Depth 


SEN RCRA WOME iid aig 8 7) Bae Nap e i ie Ot eee 10 10 
Tar Springs Sandstone (99 feet). 
re OCS WE ay (cho eras Ahern 6 MWe cl OM Aaya mt eign Re dae Zot Oe 25 3D 
Wihitersandstone was: vest. vee) Ore areas, eee eae 74 109 
Glen Dean Limestone (106 feet). 
Grayecrystalline limestone ores se ee 25 134 
Gray shale with some limestone ...........0002......... 8) 189 
Grayectysta bine MlImMestonew. «25. ase ere 26 215 
Hardinsburg Sandstone (35 feet). 
Gray slo” white sandsionem,. As. sees eae 25 240 
Grayasandy esha lates see 2) Fer 2 ete ease 10 250 
Golconda Limestone (127 feet). 
Graves LIMESTONE ee ae ae oa ee 5 255 
Gray shale with thin limestone layers ............ 25 280 
Gray limestone with some shale ........................ 61 341 
Grayeandeblack shales 5...ceet a eee ee eee ee 8 349 
Limestones and esnale. 2254 .c coe eee ee 8 304 
Gla VaerS Das ee asks See id, aoc ge ee ee 5 362 
GYaVeAIMesSlOTe cee kes Moy ee ae wae, Vice reaps wee oa 10 372 
Shake amd S117 OS LOU te soe orcas ee ee eee 5 377 
Cypress Sandstone (25 feet). 
Gray, 1O,ereen shales with«sand 722-2 o 382 
Grays POPGCi oS ALO, 2 etercet sete aacaer eect cee es 5 387 
Fine ‘red. to) 2tay Maa ndstone Ae tke eee 10 aoe 
Greenish-gray siliceous shale ...........02......4...-202--- D 402 
Paint Creek Limestone (95 feet). 
Grayecrystallinermimestonen cr. ee eee. 30 432 
Shaly limestone and siliceous shale .................. 10 442 
Gray crystalline and oolitic limestone ............ 30 472 
DarkerGalcarcous sla le stress. eens ee tee eee 10 482 
Gray crystalline limestone and shale .............. 13 497 
Bethel Sandstone (46 feet). Much gas. 
Fine, light gray to white sandstone.................. 46 543 


Renault limestone (61 feet). 
Compact and crystalline gray limestone with 
SONG sNalec, DEGSt 22sec ae eee ee 61 604 








* The writer is deeply indebted to Mr. Hynes for a very complete ser- 
ies of cuttings from this well. They were not available for study until 
after the preparation and submission of the present report, so that the 
findings could not be included in the discussion of the several Chester 
and other formations which have gone before. The importance of the 
data, however, warrants their consideration at this place. 


STRUCTURAL GEOLOGY 103 
Thickness Depth 
Ste. Genevieve Limestone. 
Lower Ohara Member (28 feet). 
Compact to crystalline, partly oolitic, gray 


NESW TL EO M1 LPULOS EOD Cate sers acta tee staee ce hn ca ccd ee 28 632 
Rosiclare Sandstone Member (13 feet). 
Mine Calva POOUS SaANUSLONG s o.202 en es fap cones vee 13 645 
Fredonia Limestone Member (371 feet). 
White oolitic and crystalline limestone .......... 48 693 
Fine white calcareous sandstone ....................-... 5 698 
Gray, yellow and white oolitic limestone with 
SUT CCH OGL sane te cadena aes oS A ith NL 35 733 
Binleservray calcareous Sandstone. .2..f2i0..... 0.0058 3 742 
Gray to white, crystalline, compact and oolitic 
limestone with some chert ........................ 274 1016 


St. Louis Limestone (335 feet). 
Light to dark gray crystalline and compact 


PIMeSLOMEsWEOM ae CUCT be 3.0 );:2.e20- ce al ascass 144 1160 
Atk raVeEcdeMIaAck +) LIIMeSstONe. _aiiehelsis---cceeteuece 128 1288 
PR eiicas ATS CCC eet eee oo co eT 63 1351 


This log has furnished important information concerning 
the thickness and lithologic character of the Chester formations 
beneath the Tar Springs Sandstone, and these thicknesses do 
not agree entirely with those determined from surface outcrops 
nor with the predictions made in the earlier description of the 
Farmersville dome. 

The total thickness of the Tar Springs Sandstone is not 
represented in the well section, but all of the Chester formations 
subjacent to the Tar Springs have been penetrated. The Glen 
Dean limestone in the section has a thickness of 106 feet, while 
in the Walche’s Cut section a thickness of 87 feet has been as- 
signed to the same formation. On the other hand the Hardins- 
bure sandstone in the well section is 35 feet while in Walche’s 
Cut 61 feet are referred to the formation. The combined thick- 
nesses of the two formations, however, in the two sections are not 
very different, 141 in the well section and 148 in Walche’s Cut. 
This would suggest that some of the higher portion of the 
Hardinsburg of Walche’s Cut, that portion with calcareous 
layers in the sandstone and shale, should more properly be trans- 
ferred to the Glen Dean limestone. 

The 127 feet of shales and limestone of the Goleonda forma- 
tion are much thicker in the well section than in most other 


104 PRINCETON QUADRANGLE 





portions of the quadrangle. In Walche’s Cut 80 feet of beds 
were included in the formation, and the minimum thickness of 
the formation seems to be as little as 30 feet. However this well 
section is the most westerly locality in the quadrangle where we 
have any knowledge of the formation, and still farther west in 
Crittenden and Livingston counties and in Illinois, the forma- 
tion attains a much greater thickness in places, than that 
shown in thé well record. This greatly varying thickness of 
the Golconda formation is doubtless due to pre-Hardinsburg 
erosion. 

Information concerning the Cypress sandstone furnished 
by the well section conforms to that derived from a study of 
the surface outcrops in the quadrangle. The formation is only 
25 feet in thickness and is very different in character from the 
massive sandstone which represents the formation farther west, 
both in Kentucky and in southern [lhinois. 

The Paint Creek limestone and the Bethel sandstone, as 
represented in the well section, conform closely with the surface 
outcrops of the same formations in the quadrangle, both in thick- 
ness and in lithologie characters. 

The Renault limestone, 61 feet thick, is a little thinner in 
the well log than the estimated thickness of about 80 feet from 
surface outcrops, but it is difficult to determine from the well 
cuttings alone exactly where the line between the Renault and 
the Ste. Genevieve limestone should be drawn. This line has 
been assumed to be between the more shaly beds of the higher 
formation and the more or less oolitic limestone below. If the 
same section could be studied in surface outcrops it is possible 
that the line would have to be shifted somewhat. 

The characteristic features of the Ste. Genevieve limestone 
are clearly shown in the well cuttings, the gray to white lime- 
stones with much oolite being a conspicuous feature. The Lower 
Ohara member is apparently about 28 feet thick. The Rosiclare 
sandstone member is entirely characteristic, with a thickness of 
13 feet. A feature of the Fredonia limestone member, with a 
total thickness of perhaps 371 feet, is the presence of two thin, 
calcareous, sandstone beds beneath the Rosiclare, one 5 feet and 
the other 9 feet in thickness. A sub-Rosiclare sandstone membe” 
of the Ste. Genevieve limestone has been recognized at a number 


STRUCTURAL GEOLOGY 105 








of localities in southern Illinois, but two such layers have not 
hitherto been observed. The total thickness of the Ste. Genevieve 
limestone, 412 feet, seems to be excessive. The line between the 
Ste. Genevieve and the St. Louis has been drawn below the last 
oolite, but it is even more difficult to recognize the line of separa- 
tion between these two formations from the well cuttines than it 
is in surface outcrops where the fossils can be appealed to. 
There is no stratigraphic interruption in passing from one 
formation to the other, and the change in lithologic character 
iS progressive. 

The St. Louis limestone, as the log is interpreted, is repre- 
sented by 535 feet of limestone, to the bottom of the well, which 
is probably near the base of the formation. The dark limestone 
of this portion of the section is characteristic of the St. Louis 
where the formation occurs in surface outerops in this portion 


of Kentucky. 
Manuscript completed Oct. 1, 1922. 


Va ~ 
; }) 


Nb 2 


ot 
4 
The four following 
papers are separate 
and unrelated to each 
other or the preceding 
report which lends its 
title to this volume. 





II. 
RECENT CAVE EXPLORATIONS IN KENTUCKY FOR 
ANIMAL AND HUMAN REMAINS 
By ArtHur McQuiston MILLER 
Assistant Geologist 


Explorations at Big Bone Lick. Upwards of a century ago 
interest in the remains of extinet animals and of man in Ken- 
tucky was much more pronounced than in recent years. Hxcava- 
tions at Big Bone Lick in Boone County for such remains— 
chiefly those of the mastodon—was a favorite pastime for such 
prominent personages as General William Henry Harrison 
(1795), Doctor Goforth of Cincinnati (1804), President Thomas 
Jefferson (1807), and John Chiford of Lexington (1816-17). 
Large numbers of remains of this extinet form of elephant— 
the mastodon—together with those of the buffalo belonging to 
living and extinet species, of the megalonyx—an extinct form 
of ground sloth—and of other herbivors which were attracted 
to such salines as this famous lick on account of the salt which 
there impregnated the soil, were exhumed as the result of these 
excavations and went to enrich the various museums of this 
country and of Europe. None of them remained in Kentucky. . 

Remains Found m Caves. Also remains were found in 
eaves as the result of excavations carried on for saltpeter at 
that period. Some of these were human. With the decline of 
the saltpeter industry after the War of 1812, few instances are 
recorded of the finding of such remains, and interest in them 
languished. 

Recent Cave Hxploration. Prompted by a knowledge of 
what was formerly obtained from the caves of Kentucky and 
encouraged by the suggestions of a leading archaeologist—Dr. 
N. C. Nelson of the American Museum of Natural History, New 
York City—to the effect that on account of the similarity of 
position with reference to the glacial drift to the north, the 
eaves of Kentucky should offer as good a field for archaeological 
exploration as those of France, the writer, in 1921, began some 
investigations on eaves, first in the vicinity of Lexington and 
later in southern Kentucky—particularly in the county of 
Wayne. While the investigations have thus. far not revealed 


108 RECENT CAVE EXPLORATIONS IN KENTUCKY 





the presence of undoubted remains of extinct animals in these 
eaves, nor of those of man of a race more primitive than the 
American Indian, they have fully established the fact that the 
caves and rock shelters of Kentucky were for a lone period 
frequented by both man and the lower animals contemporary 
with him, and that.their remains have been preserved in them 
in abundance. 


CAVES OF THE BLUEGRASS REGION 


The caves near Lexington are in limestone of Champlainian 
(that is, lower Ordovician) age, this being the only limestone 
in north central Kentucky of sufficient purity for any great 
depth to readily dissolve by percolating underground water 
so as to form subterranean passages extensive enough to deserve 
the designation ‘‘caves.’’ As this Champlainian, mainly Tren- 
ton, limestone forms by its outcrop the ‘‘Inner Bluegrass 
Region,’’ it follows that these caves are confined in north central 
Kentucky to this distinctive physiographie district. 

The Breck Smith and Phelps Caves. Two eaves—the Breck 
Smith, eight miles west of Lexington on the Old Frankfort 
Pike, and the Phelps eave, four miles southwest of the eity— 
have thus far proven to be the most favorable for exploration. 
From the former—a newly discovered cave which had pre- 
viously escaped detection because filled to the roof with earth— 
have been obtained remains of the following mammals: raccoon, 
eroundhog, gray fox (of a variety now extinct in the region), 
deer, buffalo, bear, dog or wolf, and man (Indian). Though 
doubtless some of these remains are of considerable age, esti- 
mated in years, none of them appear to date back of the present 
geological epoch. 

In a recently discovered extension of the Phelps cave there 
was found a considerable portion of the skeleton of the black 
bear, which from the alteration it had undergone and the fact 
that it was cemented together in places with stalagmitic mate- 
rial, indicated for it a greater age than any of the remains 
found in the Breck Smith cave. It is probable that this bear 
dates back to the Pleistocene. 

Quite recently a newly discovered cave on Jessamine Creek, 
not far from Wilmore in Jessamine County, has yielded some 


ce 


CAVES OF SOUTHERN KENTUCKY 109 








bone and teeth fragments which mark it as a place for further 
exploration. One of the teeth is the incisor of a very large 
-lbeaver. The cave is in the Highbridge limestone. 


CAVES OF SOUTHERN KENTUCKY 


The eavernous limestone district of southern Kentucky 
abounds in eaves and rock shelters which offer an attractive field 
for paleontological and archaeological exploration. During the 
summer of 1919 the writer, while making a geological survey 
of Allen County for the State Department of Geology and For- 
estry, discovered a rock shelter overlooking the Barren River 
containing Indian graves. Reference to this is made in the 
report on Allen County (Kentucky Department of Geology and 
Forestry, Series 5, Vol. 2, No. 3, pp. 220-242, 1919). 

The Hines Cave. During the past summer the writer, 
while on a trip to Wayne County as guest of the Michigan 
Summer School of Geology with its camp on the Cumberland 
River at Mill Springs, had opportunity to examine the region 
for caves and rock houses containing human and animal remains. 
The one which offered the best prospect was a cave on the farm 
of Honorable J. S. Hines at Mill Springs. This cave, or more 
properly a ‘‘rock house,’’ with southwestern exposure, is 145 
feet deep, 60 feet wide and 30 feet high. It is in a cliff of Ste. 
Genevieve limestone on the south side of a knob one and one- 
quarter miles due east of Mill Springs. It is evidently one of 
those “‘dry caves containing human bones,’’ which, according 
to Judge Haywood’s History of Tennessee, published in 1823, 
the party of hunters under the leadership of Kasper Mansko 
(Mansker) found in this portion of Kentucky in 1769. This 
party, by some historians identified with the ‘‘Long Hunters,”’ 
but by others called the ‘‘ predecessors of the Long Hunters,’’ 
here broke out of the forest through which they had been travel- 
ing since they left Virginia and North Carolina and saw stretch- 
ing before them to the west a great grassy, treeless plain teem- 
ing with herds of buffalo, deer and other game. Unacquainted 
as yet with the French word ‘‘prairie’’ for such a treeless 
expanse, they called it ‘‘meadow.’’ This was the eastern end 
of the strip of treeless country in southern Kentucky and north- 


Ps 


110 RECENT CAVE EXPLORATIONS IN KENTUCKY 








HINES’ CAVE, NHAR MILL SPRINGS, WAYNE COUNTY, hove 


View showing site of removed stalagmite as seen from cave entrance. 
Photo “bye. Ar tiie 2M ail eran A oat Si eae 
ern Tennessee, which later (by 1800) became known as the 
‘*Barrens.’’ At the eastern margin of this strip these hunters 
established a central eamp, called by them a ‘‘station camp,’’ 
from which they radiated on hunting expeditions and to which 
they returned every five weeks to deposit their skins. The spring 
beside which the camp. was established ean still be identified. 
It is the family spring beside the home of Tilden East. It is 
one and one-half miles a little east of south of the J. S. Hines 
cave. The first permanent settlement of Wayne County, known 
as ‘‘Price’s Meadow”’ or ‘‘Price’s Settlement,’’ was established 
here at least as early as 1797, for a map of Kentucky published 
between 1794 and 1797 by J. Russell has ‘‘ Price’s Settlement”’ 
marked upon it at this point. It is referred to under the name 
‘‘Price’s Meadow’’ by Judge Haywood in his History of Ten- 
nessee, above mentioned. The creek that drains this fine level 
tract of Jand extending to the foot of the mountains is still 
known as ‘‘Meadow Creek.’’ 
The floor of the Hines eave is covered with earth which 
contains a good percentage of nitrates (calcium and potassium 


CAVES OF SOUTHERN KENTUCKY Ee 


nitrate 2.2 per cent) along with some phosphoric acid (1.49° 
per cent). As it contains in addition a large percentage (70.6: 
per cent) of acidity neutralizing calcium carbonate it would 
make a good all around fertilizer to spread upon land just as. 
it is. The surface portion of this earthy accumulation was taken: 
off during the Civil War and leached in the cave for the nitrates: 
that it contained. Both the leached and unleached portions of 
this earthy material are filled with the bones of wild animals 
and the bones, implements and ornaments of humans (Indians). 

In the deeper portions of the earth, that lying below the 
level removed for saltpeter manufacture, are whole skeletons of 
Indians whose bodies were placed there by burial. Evidence of 
thirteen of these distinct burials was obtained. Some of the 
skeletons were in an excellent state of preservation, and were 
exhumed practically complete. They are of persons of various 
ages from extreme youth to extreme old age, and of both sexes. 
Necklaces of shells (river gastropods) had surrounded the necks: 





INDIAN SKELETON IN BURIAL POSITION. 
This skeleton was found three feet: below top of earth floor, Hines’ 


Cave, near Mill Springs, Wayne County, Kentucky. Photo by Dr. A. S. 
Hendrick, Oct... 1922. 





pele RECENT CAVE EXPLORATIONS IN KENTUCKY 








——$—» 


of some of these—probably the females. Implements, both of 
stone and bone, and burnt clay utensils (pottery) had been 
buried with them. 

The bones of the wild animals scattered through the earth 
in great profusion, from their broken condition, evidently 
belonged to those which were used for food by the inhabitants 
of this cave. All the long bones had been broken for the marrow 
and the skulls for their brain contents. These bones are now 
beine studied in the Departments of Geology and. Zoology at 
the University of Kentucky. So far, there have been identified 
from them those of mammals (deer, buffalo, bear, elk, raccoon, 
opossum, various rodents, including the beaver, wolf or dog, 
fox, wildcat, panther), birds (wild turkey, prairie chicken, 
crane), reptiles (land terrapin), fish (gar pike), and molluses 
(river mussels and snails). 

The bone implements found consist mainly of awls together 
with some needles. The former had been made from the cannon 
bones and ulnas of the deer. The stone implements consist of 
hoes (most numerous), skinners, pestles and arrow points. The 
_last are of flint; the remainder are of the native limestone. The 
pottery—all in fragments—is a coarse variety made of mixed 
elay and crushed mussel shells which had been baked after 
being molded into form by being plastered on the inside of 
basketry. The ornaments found consist of shell beads and 
trinkets made from bone, mussel shell and stone, and of a piece 
of mica—the latter evidently imported from some point out- 
side of the state. 

It is evident that the mass of the accumulated material of 
this eave constitutes a large kitchen midden—Danish kjokken- 
moddings (kitchen leavings)—and gives proof of very long 
residence of this rock shelter by the Indian inhabitants. Con- 
firmatory proof of long occupation was furnished by a large 
mass of stalagmite which was removed from the middle of the 
front portion of the shelter. This mass of calcium carbonate, 
rising above the floor in a stool three feet wide and four feet 
high, was found to expand under the soft earthy floor to a 
diameter of about eight feet and to extend downward four feet. 
After removal of this mass weighing tons, by sledge, pick and 
crowbar, excavation was made to a still further depth of four 


CAVES OF SOUTHERN KENTUCKY 113 





feet without reaching the original rock floor. <All through this 
mass and in the earth beneath, the same type of animal remains 
and articles of human workmanship were found as in the rest 
of the eave earth of this rock shelter. This stalagmitic mass 
was formed by deposit of lime from water slowly dripping from 
the roof. At present this roof drip takes place only after heavy 
rains. 

The excavation in this cave was done during two trips, one 
in August, 1922, when for ten days the party camped near the 
entrance, and the other in October, 1922, when the party worked 
out from Burnside during a week-end. Associated with the 
writer in this work were the following persons: Professors 
W.S. Webb, J. Morton Davis, W. D. Funkhouser, J. K. Mitchell, 
and Messrs. J W McCollum and Leland Snoddy from the State 
University, Major Victor K. Dodge, Dr. A. S. Hendrick; Dr. 
W. &E. Tait and William Lowry from Lexington, and Mr. C. F. 
Bales from Louisville. 

Manuscript completed Nov. 15, 1922. 


- 
N. J 
rd 








Ik. 


A POTTSVILLE-FILLED CHANNEL IN THE 
MISSISSIPPIAN 


By WiLBuR GREELEY BuRROUGHS 


Assistant Geologist 


Kentucky contains an Eastern and a Western Coal Field. 
The Eastern, with an area of approximately 10,450 square miles, 
forms part of the west central portion of the great Appalachian 
Coal Field. The Western covers 4,680 square miles and lies in 
the Eastern Interior Coal Field. 

These two coal basins of Kentucky are separated by forma- 
tions of older geologic age. Northward from about North 
Latitude 37° 30” the distance between the coal fields increases, 
the Ordovician, Silurian, Devonian, and Mississippian forma- 
tions being at the surface in various areas. Southward from 
about this line, the Mississippian formations compose the bedrock 
except where some streams have cut down locally to the Devon- 
ian. The Cumberland, Fishing Creek, and a few other rivers 
have still further increased their channels and have exposed 
the Ordovician. 

The shortest distance from the main body of Pennsylvanian 
strata of the Western Coal Basin to that of the Eastern Coal 
Basin is a straight line drawn from the main Pennsylvanian 
rocks of Hart County to the main body of these formations in 
Clinton County, a distance of about 64 miles. Measured to 
Wayne County, it is 70 miles, to Rockcastle County 90 miles. 
These measurements do not take into consideration outliers of 
small extent which will be referred to later. 

Geologic history. The geologie history of the region under 
discussion shows why there has been some uncertainty as to 
whether or not the Appalachian and Eastern Interior Coal 
Fields were once connected over the present State of Kentucky. 

Beginning at the close of Oswegan time of the Silurian 
System ! movements of the rocks of the earth caused the strata 
to emerge from the sea in a low anticline. Due to this and sub- 
sequent folding, an arch was developed with its axis crossing 
the Ohio River from the State of Ohio into Kentucky at Point 


1Miller, A. M., Geology of Ky. Series 5, Bull. 11, p. 54. 


\ 


116 A POTTSVILLE-FILLED CHANNEL 








Pleasant, about twenty miles above Cincinnati. Continued 
southward, the axis passes near Lexington. The anticline domes 
upward to its highest point in what is called the Jessamine 
Dome in the county of that name. From there it pitches south- 
ward to near the Kentueky-Tennessee boundary and then bows 
up into the Rutherford Dome of Tennessee. 

During Mississippian times deposition extended westward 
and possibly covered the Bluegrass. At the close of this period 
the sea withdrew from a large part of the eastern interior, 
thereby exposing the sediments which formed dry land to the 
agents of erosion. In Kentucky the strata near the crest of the 
arch were worn away first. This beveling of the Mississippian 
strata caused the various formations to outcrop in belts. Deep 
channels were worn in the Mississippian rocks. In some local- 
ities softer shales and limestones overlying the Mammoth Cave 
limestone were entirely eroded away and the Mammoth Cave 
limestone itself cut into. 

When the Pennsylvanian Period commenced, the advane- 
ing waters moving slowly westward from a region to the east 
of Kentucky, encountered a much eroded land surface inter- 
sected by river valleys. Upon this uneven surface were then 
laid down the basal rocks of the Pottsville formation. 


In some places of the United States the Pottsville is com- 
posed partly of chert derived from the Mississippian limestone. 
This indicates the great length of time the Mississippian rocks 
were being weathered before the Pottsville was laid down. The 
Pottsville varies greatly in thickness due to irregularity of the 
surface of the ‘underlying Mississippian formations, unequal 
rates and length of deposition, position relative to the shore 


line or river bank. The unconformity between the Mississippian 


and Pennsylvanian Systems spreads over a wide territory from 
Pennsylvania and Tennessee and Kentucky to Utah and 
Montana.’ | 

With the continuance of the Pennsylvanian Period exten- 
sive swampy areas came into existence and coal began to be 
formed. At the close of the Pennsylvanian the State of Ken- 
tucky was elevated never again to be completely submerged. 





Chamberlain, T.-C. and Salisbury, R, ‘‘College Geology,’’ p. 602. 


CONGLOMERATE IN ERQ@QDED MISSISSIPPIAN 117 








The enormous period of time that has elapsed since the 
close of the Pennsylvanian has permitted extensive erosion to 
take place especially along the higher portions of the Cincin- 
nati Arch in the Jessamine Dome. The result has been that the 
younger formations have been entirely worn away, exposing 
the underlying Ordovician strata and thereby forming the 
celebrated Bluegrass Region of Kentucky. The younger forma- 
tions are being eroded away in a circle from the center thus 
ever widening the area of Ordovician surface rock. The Knobs 
of Kentucky now form the fringing margin between the main 
masses of Pennsylvanian formations and the Bluegrass terri- 
tory. The present Eastern and Western Coal Fields owe their 
existence to being down on the flanks of the Cincinnati Anti- 
cline and thus they have not been eroded as rapidly as have the 
formations at or nearer the crest of the Arch. | 

But the question arises, did these two coal basins ever 
extend over the top of the Cincinnati Arch and unite to form 
one field? If they were united in Pennsylvanian times and 
since have been separated by erosion, may not there be some 
traces of their former surface area? 

roi N woe laler WM alimnney, AW. Te Knott “Acree: 
Miller and others have stated their belief that the two coal 
fields once were connected. 

Professor Shaler wrote :? ‘‘The Carboniferous conglomerate 
increases in thickness as we recede from the Cincinnati Axis. 
It contains a great quantity of pebbles, both in the east and in 
the west, but not a trace has yet been found of any pebbles 
which could be attributed to the Cincinnati axis. 

‘It is impossible to resist the conviction that a million of 
vears ago, or thereabouts, this section still contained a con- 
tinuous sheet of coal reaching from Wayne and Clinton Coun- 
ties, on the east, across to Edmonson and Hart, on the west.’’ 


POTTSVILLE CONGLOMERATE IN ERopDEp MISSISSIPPIAN 


Dr. W. R. Jillson, State Geologist of Kentucky, in May, 
1922, directed the writer to map the Pottsville in certain areas 
of central and eastern Hart County and the adjoining counties 
of Larue, Green, Taylor and Marion, where an extended area 





3 Report of Progress, Shaler, Ky. Geol. Survey, 1877, p. 17. 


SY 


118 A POTTSVILLE-FILLED CHANNEL 








of the basal formation of the coal measures was regarded as 
present. The writer started into the field at Munfordsville, 
Hart County, Kentucky. 

At Munfordsville the surface rock is Ste. Genevieve lime- 
stone of the Mammoth Cave series, Mississippian System. The 
elevation at the Munfordsville Courthouse is 571 feet above sea 
level. Along this western outcrop of the Ste. Genevieve, it gen- 
erally is a thick bedded ocolite in which are interbedded. layers 
of non-oolitic limestone. The thicker beds weather a distinctive 
white color. The Ste. Genevieve outcrops in a belt from the 
Ohio River in western Meade County southward to Tennessee, 
and east of the Bluegrass in a narrow strip from Tennessee to 
the Ohio River.’ Monticello, Somerset and Mt. Vernon are along 
this outcrop. 

Beneath the Ste. Genevieve comes the St. Louis limestone 
also of the Mammoth Cave series. It is chiefly a moderately 
thick bedded, fine grained, dark: to black limestone. Blue and 
eray layers of fine texture occur. A distinguishing mark of the 
St. Louis is the quantity of irregular surfaced flattish pieces of 
chert it contains. Abundant chert debris is seen alone the 
weathered outcrop of this formation. Also the St. Louis is non- 
politic. . Thus it differs markedly from the overlying oolitie 











Section of Pottsville filled main channel and distributary. Shows main 
stream moving up original tributary, depositing pebbles and sand in both 
channels. 

Horizontal scale 1 inch=—% mile. x 

Vertical exaggeration 8.8 times horizontal. 

t—r-——water surface of main river and its overbow into the tributary. 

Pe—Pottsville conglomerate. . 

t—channel of tributary stream. 

m—mouth of tributary where it joins main stream. 

m—r—main river. 

Mis—Mammoth Cave limestone in whose eroded surface are the chan- 
nels of the main river and its tributary. ' 

Arrows indicate direction of movement of water in main river moving 
up tributary, and flow of tributary stream before it reaches its ponded 
portion. 


Ste. Genevieve. The St. Louis starts in Kentucky in Meade 
County at the Ohio River and stretches southward through 


4Butts, Chas. ‘Mississippian Series of Eastern Ky.,” Ky. Geol. Surv., 
Series VI, p. 1388. 


CONGLOMERATE IN ERODED MISSISSIPPIAN 119 


Hardin, Larue, eastern Hart, northern Barren, eastern Warren 
and Simpson Counties. Its eastern outcrop is a rather narrow 
belt which extends through Clinton, Wayne, Pulaski (east of 
Fishing Creek), and Rockeastle Counties; northeast of Rock- 
eastle County it is not so important and thins out entirely not 
far northeast of Frenchburg, Menifee County.® 

Above the Ste. Genevieve the Cypress sandstone, Chester 
Group, Mississippian System, caps a number of the knobs lying 
near Munfordsville, and to the east. It usually is a thick 
bedded, gray sandstone. Butts states, that ‘‘in places it is 
thin bedded, has strongly cross-bedded lavers, and that in the 
vicinity of Sample and Stephensport, Breckinridge County, it 
takes on a shale facies and has very little sandstone. Some of 
the shale is red, but most of it is green. The Cypress sand- 
stone in Kentucky is mainly confined to the country west of the 
meridian of Louisville and north of the latitude of Bowling 
Green.”’ 6 

The formations just described in west central Kentucky 
he on the western flank of the Cincinnati Arch. The general 
dip is therefore westward. As one goes eastward, due to the 
beveling by erosion already referred to, older and older strata 
form the main surface rocks. Three and one-quarter miles north 
of Munfordsville, along the Louisville & Nashville Railroad, on 
the east side of the tracks, occurs a fault which has brought the 
Pottsville conglomerate down into the Mammoth Cave lime- 
stone. The limestone near the fault plane dips 24° northwest- 
ward toward the fault. About 300 feet south on the horizontal 
along the railroad tracks from the main fault a smaller fault 
has oceurred, also bringing the Pottsville down into the lime- 
stone. The fault planes extend in a general northeast-southwest 
direction. The main block of faulted conglomerate extends 
northward along the Louisville & Nashville Railroad for about 
334 miles. It forms the surface rock from the tracks to the 
top of the hills nearby. Massive Pottsville conglomerate was 
found near the summit of the high knob west of the tracks. 
Measured at right angles to the major axis of the faulted block 


> Butts, Chas. ‘‘Mississippian Series of Eastern Ky.,’ Ky, Geol. Sur- 
vey, Series VI, p. 125. 

¢ Butts, Chas. “Mississippian Series of Eastern Ky.,’’ Ky. Geol. Sur- 
vey, Series VI,: pp. 165-16. 


120 A POTTSVILLE-FILLED CHANNEL 





of Pottsville rock, the width of the block is about 3144 to 41% 
miles. 

About three-quarters of a mile north of Bonnieville, the 
north side of the faulted conglomerate is reached and Mammoth 
Cave limestone again becomes the surface rock from the rail- 
road to the tops of the gently sloping hills, except where they 
are capped by Cypress sandstone. The topography resumes 
about the same aspect it had south of the faulted area. 

West of the Louisville & Nashville tracks the writer mapped 
both sides of the down thrown Pottsville formation until it 
joined the main mass of the Pennsylvanian of the Western Coal 
Field. Mammoth Cave limestone country with wide valleys and 
comparatively gentle slopes border the rough area of the Potts- 
ville block. The Pottsville varies in thickness from being 
entirely absent to 15 feet along the sides of the lens, up to 200 
feet and over near the center. This doubtless is due to the sand 
and pebbles having been deposited in a deep channel eroded in 
the Mississippian formations. Then later the Pottsville filled 





Diagrammatic section of faulted Pottsville filled channel in eroded 
Mississippian, west of Louisville & Nashville Railroad, Hart County, 
Ky. Note eroded surface of Mammoth Cave limestone on which the con- 
glomerate rests. The Pottsville which originally extended on either side 
of the faulted area has been removed by erosion, as here illustratd. 

Horizontal scale, 1 inch==1 mile. 

Vertical exaggeration, 7.54 times horizontal. 

Pe=—Pottsville conglomerate. 

Cys-——Cypress sandstone. 

Mlis.—Mammoth Cave limestone. 


ehannel was faulted downward. Near Cub Run, on a hill to 
the northwest of the Pottsville, the formations dip southeast 
toward the Pottsville at an angle of 20 degrees. On the south- 
east side of the Pottsville on the road from Cub Run to Mun- 
fordsville a brownish gray sandstone dips at approximately the 
same angle northwest toward the Pottsville lens.- Thus the 
downthrow of the Pennsylvanian rocks caused the nearby sur- 
rounding formations to slant toward the fault area. 

About one-quarter of a mile east from the Louisville & 
Nashville tracks north of Bonnieville, on a road that leads ulti- 


CONGLOMERATE IN ERODED MISSISSIPPIAN 121 








mately to Hammonyille, on the north side of the fault block, 
oceurs a ledge of dark and heht gray limestone with beds 3 to 4 
feet thick. Total height above the road equals 20 feet. About one 
and one-half miles along this road to Hammonville, Pottsville 
pebbles occur approximately 50 feet vertically lower than the 
limestone just mentioned. Faulting and probably an erosion 
channel in the Mississippian, account for this position of the 
Pottsville in this small lens below the Mammoth Cave beds. 
Further along this road eastward occurs a small gravity fault. 
The Pottsville conglomerate, light gray oolitic Ste. Genevieve 
limestone and the darker gray, non-oolitic St. Louis limestone on 
the down-thrown side have been tilted on edge and brought 
down against other portions of the St. Louis. The distance 
across the edge, and hence the thickness of the Pottsville is 50 
feet, the Ste. Genevieve 75 feet. Chert waste occurs on the St. 
Louis upthrow side of the fault. The fault plane extends in a 
general east-west direction. 

On this same road occur red sand banks containing Potts- 
ville quartz pebbles for a thickness of 40 feet. It is bounded at 
least on one side, where it can be seen, by dark gray, massive 
St. Louis limestone. It is a channel filling in the St. Louis. 

Further on, on the outskirts of Hammonvyille, near the top 
of the hill above the stream in -the bank beside the road occur 
Pottsville pebbles. Upon digging into the bank, it is found that 
beneath the weathered exterior the conglomerate became quite 
solid, although still weathered. The formation is distinctly 
eross-bedded and has the appearance of a delta formation. It 
probably is a small distributary from the main stream in the 
eroded Mississippian. Slightly down the hill is found the chert 
waste from the St. Louis. The St. Louis in the bed of the stream 
at Hammonville is dark gray, beds 2 to 3 feet thick, dipping 
3 to 4 degrees toward the west. This St. Louis is very near 
the delta deposited Pottsville. If the Pottsville had been 
brought to its present position in this small lens by faulting, the 
St. Louis strata doubtless would have dipped at a greater angle 
than they do, and would have dipped with some relation to the 
position the Pottsville holds, but the St. Louis beds were inclined 
at the small angle mentioned, and slanted with no relation to 


122 A POTTSVILLE-FILLED CHANNEL 





the Pottsville. Hence the Pottsville acquired its present posi- 
tion as stated above. 

From Hammonville to Magnolia cherty waste from the St. 
Louis is exposed beside the road. 

On the southeast side of the large mass of Pottsville, Bett 
of the Louisville & Nashville tracks, patches of Pottsville peb- 
bles occur along the side of the main Pottsville area. They 
are separated by Mississippian waste. In all cases only masses 
of Pottsville pebbles, at least 3 to 4 feet thick in situ, were 
mapped. Care was taken not to count loose pebbles which had 
been scattered by surface waters of the present day. The natives 
call the Pottsville quartz pebbles ‘‘ Jack Rocks.’’ About four- 
fifth of a mile west of Atna Furnace, Hart County, in the bank 
beside the road, weathered Pottsville pebbles and sand come 
in sharp contact with a cherty, gray, very hard limestone—the 
St. Louis. The curve of the contact resembles the bank of a 
small stream. The west side of this apparent channel filling 
was not exposed. North of Atna Furnace, toward Larue 
County, Pottsville pebbles, bounded by cherty limestone waste, 
occur. This sort of occurrence was noted frequently. The hori- 
zontal extent of the conglomerate pebbly deposit in these small 
channels varied from 20 feet to about 300 feet. Their long 
axis apparently ran in a direction that would meet the main 
body of the Pottsville. Even this main body of conglomerate 
was patchy in eastern Hart County in places. 

The Pottsville in passing out of the northeast corner of 
Hart County cuts through the southeast corner of Larue County 
and extends in a narrow ridge, with spurs running off due to 
present stream erosion, alone the boundary of Larue, Green, 
Taylor and Marion Counties. The conglomerate here is less 
weathered in places. The ridge forms the drainage divide 
between the tributaries of Rolling Fork on the north, and those 
of Green River on the south. The topography is very rough 
and wild. The people, influenced by this Pottsville topography, 
resemble the mountaineers of the main mass of Pennsylvanian 
formations many miles away. The conglomerate and its waste 
can be traced eastward for miles. 

The distance from the end of the rather continuous Potts- 
ville to the nearest Pennsylvanian strata of the Eastern Coal 





INFLUENCE UPON LIFE OF THE PEOPLE 123 





Field is about 50 miles. Even after its continuity as a lens dis- 
appears, patches of Pottsville pebbles occur here and there from 
one coal field to the other.“ Such patches of Pottsville waste 
were noted in Lincoln County and deseribed by Linney in his 
‘*Report on Lincoln County,’’ and by Prof. A. M. Miller in the 
Bulletin of the Geological Society of America, Vol. 20, 1908. 
Green River Knob, in the south corner of Casey County, is 
capped by the Pottsville sandstone. The Cypress sandstone 
of the Mississippian, already mentioned as capping knobs, gives 
evidence of the fact that it once crossed the Cincinnati Arch and 
has since been isolated into outliers by erosion. The patches of 
Pottsville referred to above indicate that in the stream channel 
in which it was deposited, it also crossed the arch. The appear- 
ance of a stream channel filled with Pottsville sand and pebbles 
is somewhat more marked after one leaves the strikingly faulted 
portion to the west: although even there the fact that it is a 
channel filling is apparent. 

Across the interval between the coal fields, somewhat north- 
east from the Pottsville filled channel which we have been fol- 
lowing, in southeastern Madison County, is a valley worn in the 
Mississippian and filled with Pottsville conglomerate. This chan- 
nel is at present, due to erosion, at the top of the knobs. Some 
of the pebbles are as large as hen eggs. Much cross-bedding 
occurs. This Pottsville disappears on the sides of this old valley, 
but increases not entirely as conglomerate, however, to 150 feet 
at the center. It is another Pottsville filled channel similar 
to the one running eastward from Hart County. The two fill- 
ings of Pottsville might have been dsposited from the same 
drainage system. 


INFLUENCE OF THE POTTSVILLE-FILLED CHANNEL Upon THE LIFE 
OF THE PEOPLE 


The stretch of rugged Pottsville conglomerate land flanked 
on both sides by Mammoth Cave limestone territory presents a 
striking contrast not only in topography but also in the life of 
the people. The limestone areas have been worn into wide, com- 


‘Miller, A. M., “Geology of Kentucky,’’ Dept. of Geol. of Ky., Series 
Vee Bil SLT oy5..- 200: 

®* Butts, Chas., ‘Mississippian of Eastern Ky.,’ Ky. Geol. Survey, 
Ser. iVi4ds) Da 166. 


124 A POTTSVILLE-FILLED CHANNEL 





paratively gently sloping valleys. The farmhouses and barns 
are well built on the average, and often painted neatly. The 
people appear comparatively prosperous. The main roads are 
piked. 

In contrast to this peaceful scene of the limestone areas, 
the narrow rugged Pottsville formation stretches like a wall, 
where it is well developed, approximately northeast-southwest 
in Hart County. Numerous streams have dissected the con- 
elomerate into a rough, mature topography. The roads are 
often not much better than trails. They are nearly always 
ill-kept, with great holes caused by washouts and ruts worn by 
the wagons of the mountaineers. QOne-room cabins and small 
box-houses are the rule. The people are poor and appear illit- 
erate and shy. Their fields are small patches on the steep slopes 
of the unfertile soil, where they endeavor to raise tobacco and 
corn. Trachoma is present and frequently well developed, even 
to blindness. 

The people are very courteous and hospitable once their 
Inherent shyness is overcome. During the meals the mother 
and girls served the husband and his guest, as is done generally 
in the more remote parts of the southern Appalachian coal field. 
Occasionally a cabin had its walls papered with newspapers, 
Everywhere the cabins were clean. The food in this Pottsville 
belt is typical of the mountains—eges, soda biscuit, pork or 
bacon in gravy, and very strong coffee: Canned berries of 
many kinds were served, and butter, probably in honor of the 
company. 

Prof. A. M. Miller, who was in a part of this area in 1908, 
writes that ‘“It need awaken no surprise to learn that now and 
-then a wild turkey may be seen, that the wildcat is not unknown, 
and the feud not uncommon. . . .’’® The region offers an 
interesting problem for detailed geographic study. 


CONCLUSION 
The Pottsville conglomerate filled channel which we have 
traced northeast in Hart County and thence eastward toward 
the eastern coal field was probably formed as follows: (1) At. 


* 9 ee A M., “Geology of Ky.,’’ Dept. of Geol. of Ky., Series 5, Bull. 
Ppl Cpe 4 0) ee - 


KENTUCKY GEOLOGICAL SURVEY 
5S (ULES SERIES WZ., 1923 
W. RFR. JILLSON, STATE GEOLOGIST 


SKETCH MAP 
SHOWING EXTENT oF 


2 aa et POTTSVILLE (COAL MEASURE) SEDIMENTS 
(ee HART, GREEN, TAYLOR, MARION, AND LARUE COUNTIES, KY. 


eee GEOLOGY BY WW. G. BURROUGHS AND A. M. MILLER 


-— . d 


PE oe re ela Zee) 


PIUMFORBDOVILL 


ue 


Va Kh fac ae Nkeonnee “~___N 


: === 7 ee ee meet em as 
: 
Not Hart @ounty geology by Burroughs; Green, Larue, Taylor and Marioffounty geology by Miller. 
ote :— 





THEORY OF FORMATION—CONCLUSION 125 








the close of the Mississippian Period the land in Kentucky rose 
above the sea. The strata higher up on the Cincinnati Arch 
were worn away the most rapidly, causing the older strata to 
appear at the surface in belts. Numerous channels were worn 
in the Mississippian formations. In Pennsylvanian times waters 
of an alluvial fan advanced westward into Kentucky, slowly 
moving from regions to the east. These waters filled the ero- 
sional valleys in the Mississippian formations with sand and 
pebbles derived originally from Appalachia to the east." 

(2) In the case under consideration, two fresh water 
streams, the one flowing east and the other west, having their 
divide near the erest of the arch had eroded their drainage 
patterns in the surficial Mississippian. The Pennsylvanian 
waters in time filled these valleys and gradually passed over the 
main divide between them;:forming one continuous coal measure 
stream flowing from eastern: to western Kentucky. The waters 
of this-.large stream’ were impounded in-the many branch val- 
levs of the former streams until they overflowed through low 
passes into the lower lands and other tributaries which they 
found and then spread out as distributaries over the land sur- 
face. Sand and pebbles were laid down, filling the branch 
channels as well as the main river. The sand and pebbles were 
often deposited with cross-bedding. In some places larger 
rounded quartz pebbles were dropped and the finer sand sorted 
out, and to a great extent carried away. If the waters covered 
the land between the distributaries, they doubtless were not 
very deep and the sediments they deposited not very thick. 
Higher knobs of Mississippian formations may have stood as 
islands above the swirling waters. But a connection was made 
between what is now the Eastern and Western Coal Fields and, 
therefore, between the Appalachian and Eastern Interior Coal 
Fields, by the Pottsville sediments laid down in this great valley. 

(3) The channel filled with Pottsville rock was subsequently 
faulted downward into the surrounding Mississippian forma- 
tions. This aided in preserving the Pottsville from erosion, in 
addition to its favorable position in the channel carved in the 
Mississippian strata. } | 





10 Graham, Vege Lextbook of Geolocy. Part Il,1921, p. 479. 


126 A POTTSVILLE-FILLED CHANNEL 








(4) At the close of the Pennsylvanian all of central and 
eastern Kentucky was elevated never to go beneath the water 
again. During this lapse of time the rocks near the crest of 
the Cincinnati Arch have suffered the greatest erosion Those 
situated farther down the sides of the fold and in the synclines 
have been more or less preserved. Today near the crest of the 
Arch only the channels filled with Pottsville remain. The more 
exposed limestone on the sides of the channels have been worn 
away, leaving the Pottsville channel fillings, where thick, stand- 
Ing up above the surrounding country. 

(5) The Pottsville filled channel here described has influ- 
enced strikingly the life of the people who inhabit its areas. 
They resemble in all respects the people of the Pottsville coun- 
try of the Eastern Coal Field. This ancient connection between 
the Eastern and Western Coal Fields, although obliterated in 
parts, still forms a connecting link by determining that the life 
of the people within its boundaries shall be that of the Potts- 


)ille coal fields. 
Manuscript completed January 12, 1923. 


\ 
yy 


“ES 
(Z 
Sw 


AVA 
THE FLORA OF THE WESTERN KENTUCKY COAL 
FIELD 
By ApoupH CHARLES NOE 
Paleobotanist 
THe LITERATURE. 

The fossil flora of the western Kentucky coal fields was 
first examined by Leo Lesquereux! in 1857. He describes the 
various coal seams which he studied and lists the fossils found 
with each one of them. Since that time our knowledge of fossil 





1. COAL BALL FROM WEST KENTUCKY MINE NO. 12. 


plants has considerably increased and the terminology of paleo- 
botany has been somewhat revised and changed. His nomen- 
clature does therefore no longer correspond, in many eases, with 
that of today, and his species names must be accepted with 
reservations. Otherwise Lesquereux’s work is an excellent piece 
of paleontological research and a fine testimony to his knowl- 


1Leo Lesquereux, Paleontological Report of the Fossil Flora of the 
Coal Measures of the Western Kentucky Coal Fields (Third Report of the 
Geological Survey in Kentucky, made during the years 1856 and 1857 by 
Dy sO wenoehrankrtort, sod, 8pp., 499-556) plasVil. ViIl-- 


128 FLORA OF WESTERN KENTUCKY COALS 





edge of fossil plants. He was the great pioneer of paleobotany 
in the United States, whither he came with his fellow-country- 
man, the famous Louis Agassiz. In 1859 Lesquereux? continued 
his investigation of coal plants in Kentucky, extending it to 
eastern Kentucky as well. 





2. IDEAL COAL-MEASURE SWAMP IN KHEINTUCKY. 


Lester F. Ward? of the United States Geological Survey 
treats fossil plant deposits in Kentucky in a few pages of his 
large report on the geographical distribution of the fossil plants 
in North America. 

Since that time only sporadic information on fossil plants 
was given in various short passages in the ditetent bulletins of 
the Geological Survey of Kentucky. 


THE CARBONIFEROUS PERIOD 


The carboniferous period is divided in Kentucky as else- 
where in North America into the Mississippian and the Penn- 


* Leo Lesquereux, Report of the Fossil Flora and of the Stratigraphical 
Distribution of the Coal in the Kentucky Coal Fields (Fourth Report of 
the Geological Survey in Kentucky made during the years 1858 and 1859 by 
D. D. Owen, Frankfort, 1861, pp. 3833-487, pl. I-1V). 

31889, Lester E. Ward, The NS Sekt oe distribution of fossil plants 
(EFighth Annual Report of the U. S. Geological Survey 1886-1887 by J. W. 
eet Washington, 1889, Part II, pp. 663-960, pl. LXI.), Kentucky, pp. 

Vf ad 84, 


THE CARBONIFEROUS PERIOD 129 


sylvanian Systems. The main bulk of the Carboniferous flora 
is found in the latter system because it contains the Productive 





3. LEPIDODENDRON VOLKMANNIANUM FROM PRINCETON, KY. 


Coal Measures, with their wealth of plant hfe. Only a few 
specimens from the Chester series of the Mississippian were 
collected during these investigations. 


In the following a rather full picture of the Pennsylvanian 
plant life is attempted in order to familiarize the public with 
the principal types of the coal flora and to increase its interest 
and cooperation in future collecting expeditions. 

The fossils appear either as petrefacts when the plant tissue 
is well preserved by impregnation with calcium and silicon or 
they are mere impressions and casts in the shale or sandstone. 
Petrefacts may be either petrified pieces of wood or coal balls. 
The former are found frequently in the fossiliferous strata, but 
coal balls had not been reported previously in American deposits. 
They are black or brown pieces of rock containing well-preserved 
stems, roots, fructifications, and leaves which had formed part 
of a coal producing layer of plant matter but were preserved 
-as plant individuals by an early infiltration with lime or 
silicon. 


130 FLORA OF WESTERN KENTUCKY COALS 











4. LEPIDODENDRON VOLKMANNIANUM: FROM PRINCETON, KY. 


Coal is metamorphosed and amorph plant matter, which 
shows cell structure only in rare circumstances under the micro- 
scope. But the coal ball can be cut and ground to microscope 

~slices and will allow examination at a linear magnification of 
several hundred times, just like tissues of living plants. There- 
fore, coal balls are of greatest importance in fossil botany. 
They have revealed the wonders of paleozoie plant histology. 
Up to the present coal balls have only been found in England, 
France and the coal fields of Silesia and Moravia. The writer 
has been constantly on search for coal balls in this country. 
Many pyritie coneretions (nigger-heads) occur in the coal, but. 
the pure caleareous or siliceous type which is suitable for micro- 
scopic examination in transparent light could not be located. 


THE CARBONIFEROUS PERIOD 131 











5. LEPIDODENDRON VELTHEIMIANUM FROM PRINCETON, KY. 


The first discovery of a real American coal ball occurred in Mine 
No. 12 of the West Kentucky Coal Company near Sturgis, 
Kentucky. The coal ball (Fig. 1) is unusually large as com- 
pared with the Kuropean material and promises to give valuable 
information when it will be cut. 





6. LEPIDODENDRON VELTHEIMIANUM FROM PRINCETON, KY. 


132 FLORA OF WESTERN KENTUCKY COALS 





Since coal balls are caleareous concretions found in the 
coal seam they were rather expected to occur in the Kentucky 
coal No. 11 and the coresponding coal No. 6 of Illinois, which 
have a limestone cap rock. But the coal ball from Sturgis was 
found in coal No. 9 and similar coal balls were found in [hnois 
in coal No. 5 (O’Gara Mine No. 9 in Harrisburg’). Investigation 
must therefore be prepared to look for such balls in these two 
corresponding seams of Kentucky and Illinois. There will be 
found, among the illustrations to this paper, some. microphoto- 
eraphs obtained from [Enelish coal balls. They were taken by 
Dr. Paul Sedgewick in the botanical laboratories of the Uni- 
versity of Chicago and prove the importance of this source of 
paleozoic plant material to science. 

All illustrations of fossil plants are reproduced from orig- 
inals which were collected by the writer or by other persons 





7. LEPIDODENDRON FROM PRINCETON, KY. 


connected with the Walker Museum of Paleontology in the Uni- 
versity of Chicago. The habit pictures of fossil plants were 


THE CARBONIFEROUS PERIOD 133 








taken by Dr. Lillian Reynolds of the University of Chicago. 
Wherever possible Kentucky fossils are presented, but in a few 
instances fossils from Braidwood, Mazon Creek, and Spring 
Valley in Illinois were included in order to illustrate the type 
of flora which covered the great basin of Kentucky, Illinois and 
Indiana in Pennsylvanian times. 

The field work upon which this report is based began July 
28, at the suggestion of Dr. W. R. Jillson, State Geologist, and 
ended August 27, 1922. Mines and outcrops were visited in 
Caldwell, Union, Henderson, Daviess, Webster and Hopkins 
Counties. Owing to the shortness of time a number of impor- 
tant localities in Haneock, Ohio, McLean, Muhlenberg, Breck- 
inridge and Butler Counties could not be seen during this year’s 
trip. 





8. DECORTICATED LEPIDODENDRON STEM FROM PRINCETON, KY. 


The Survey is indebted in many ways to the citizens of these 
regions generally for their cheerful cooperation in furthering 
the work and especially to the Hon. G. L. Drury of Morgan- 
field, to Mr. J. C. Jenkins of Henderson, to the Bell Coal & 
Navigation Company, the West Kentucky Coal Company, the 
Morganfield Coal & Coke Company, the Southland Coal Com- 
pany, and to numerous other corporations and individuals. 


134 FLORA OF WESTERN KENTUCKY COALS 





A WESTERN KENTUCKY CoAL Swamp DuRING THE 
PENNSYLVANIAN PERIOD 
An ideal landscape showing the vegetation during the 
Pennslyvanian period in Kentucky gives us a startling picture 
(Fig. 2). Big trees which were probably over one hundred feet 
high, in many instances, form the bulk of the swamp forest. 
They belong to the extinct genera of Lepidodendron and Sigil- 
laria whose surviving relatives are the small clubmosses (lyco- 
podium and Selaginella). These trees alternated: with groups 





9. DECORTICATED LEPIDODENDRON STEM FROM PRINCETON, KY. 


of gigantic horse tails (Calamites) of from twenty to thirty 
feet in height. Also some true Gymnospermie trees related to 
our pines and hemlocks were among the forest trees. The under- 
brush consisted of ferns and cyeade-like, medium sized shrubs. 
The water currents are full of a, long since, extinct type of 
plants, the wedge shaped Sphenophyllum. Various climbing 
ferns cover the large trees and the open spaces in ‘the~ thick 
forests are dotted with fern trees, some of which bore seeds. 
This great swamp vegetation of western Kentticky; Tlinois 
and southwestern Indiana grew at a low mean sea level‘and was 
frequently subjected to inundation. Sometimes the swamp was 
filed up with the stagnant waters of rivers when these were 
obstructed in their course by sandbars. In such a ease it was 


PLANT GENERA OF WESTERN COAL FIELD 135 





a fresh water inundation. At other times the sea level rose and 
in the course of thousands of years the ocean water covered the 
swampy plains. More frequently it may have been the brackish 
water of the river deltas which flowed back into the land and 
covered everything with its salty floods. Whenever such an 
inundation occurred the rich vegetation was buried in sand 
and mud. Again the water level sank and a new vegetation 
occupied the.emerged lowlands. 





10. DECORTICATED LEPIDODENDRON STEM FROM PRINCETON, KY. 


Submersions and emergions alternated successively many 
times and left as many layers of vegetable matter burried under- 
eround. The pressure of the overlying masses transformed the 
plant masses into coal, and a series of successive coal seams 
resulted. The plant structure disappeared in the coal, but 
many individual plants or plantorgans had been separated from 
the great mass and were buried in the sandstone or shale cover 
of the coal seam. They became imprints in the rocks, forming 
the roof of the coal, and in that way preserved their individual- 
itv. Other masses of vegetable matter were saturated with lime 
or silicon and became coal balls. Out of the impressions in the 
shales and sandstones and from microscopic sections of coal 
balls we have gained our knowledge of the vegetation which 
filled once the coal swamps of North America and we were able 
to reconstruct a picture of the swamp forests which once covered 
the basin of western Kentucky, [linois and Indiana. 


PLANT GENERA OF THE WESTERN KENTUCKY CoAL FIELD 

A true conception of a coal swamp flora is best obtained by 
an examination of the fossil evidence. Herewith is given a 
description of the fossil types which lead to such a reconstrue- 








Pees, 
0 
has 


8. 
Lg 

88 
if 


4 
8 
. 3 

rt 
segs 


iJ 
iP 


eee 
St ge 4 
Pes 


ie 

Beg td 

hg hog tei Me sh 
ies: 
sitet 


ee 





11. TRANSVERSE CUT OF BRANCHING: LEPIDODENDRON STEM 
FROM COAL BALL. 


tion. The types described were all found in western Kentucky 
in the course of the field work of last summer. 

The largest tree forms belonged to two families represented 
by the genera Lepidodendron and Sigillaria.  Lepidodendron 
means ‘‘Scale’’ tree because its bark looked like a fish scale. 
Figures 3 and 4 show an early type of Lepidodendron (L. Volk- 
mannianum Sternb.) found in the Tar Springs sandstone, three 
and one-half miles northeast of Princeton, Kentucky. The 
scale-like bark appears very clearly. The leaf cushions forming 
the bark are still comparatively simple. The Tar Springs sand- 
stone at the point where these fossils were taken les below the 
Pennsylvanian or the so-called Productive Coal-Measures and 
is a member of the Mississippian series. 


? 


PLANT GENERA OF WESTERN COAL FIELD 137 











12. LEPIDODENDRON LEAVES FROM PRINCETON, KY. 


The design of the bark in Figures 5 and 6 is more orna- 
mental. These photographs represent specimens of a Pottsville 
species (Lepidedendron Veltheimianum Sternb.). The Potts- 
ville forms the lowest portion of the Pennsylvanian series. Fig- 
ure 5. which is a positive east, was found eleven miles northwest 
of Princeton, Kentucky, while a corresponding negative cast 
(Fig. 6) was picked up along the old road at the forking of 
Piney Creek, twelve miles southwest of Providence, Kentucky. 


Figure 7 shows a specimen from the same locality as Figures 
38 and 4. The stem to the right is a well preserved cast of 





13. SIGILLARIA STEM FROM BARLINGTON, KY. 


138 FLORA OF WESTERN KENTUCKY COALS 
Lepidodendron obovatum, Sternb., while the one to the left had 
suffered to a considerable degree decortication, which means 
the tree trunk had been washed about by current water and 
the outer bark or cortex had been shorn off before the specimen 
became embedded in the sandstone. Figure 8 represents another 
decorticated stem, probably from L. Volkmannianum, and was 
found in the same place with the specimens illustrated by Fig- 
ure 5. 

Decortication had proceeded so far in Figure 9 as to remove 
the entire bark of the specimen. In this instance the inner as 
well as the outer cortex is gone. The specimen was found on 
Piney Creek near the locality of the specimen shown in Figure 
6. It 1s impossible to determine with accuracy the spe-ies of 
the specimen shown in Figure 9, but it might have been L. Volk- 





14. STIGMARIA FUCOIDES FROM HENDERSON, KY. 


PLANT GENERA OF WESTERN COAL FIELD 139 





mannianum. Another decorticated specimen, a cast of a small 
tree trunk which probably belonged to L. obovatum, is found in 
Figure 10. It comes from the same bed as Figures 5, 7 and 8. 
The Lepidodendron stem is divided dichotomously, that is, it 
branched by repeated forking. This is very well illustrated in 
a microphotograph taken from an Hneglish coal ball (Fig. 11). 
The leaves of Lepidodendron were lanceolate, somewhat resem- 
bline grass blades, and stood in tufts on the younger branches 
of the trees. Figure 12 represents a layer of these leaves, which 
was found in the same place with the specimen of Figure 3. 
To the ends of the voune branches were attached the spore bear- 
ine cones of the Lepidodendron tree. They are rarely found. 
Similar in size was another great tree of the Coal-Measures, 
the Sigillaria or ‘‘Seal’’ tree, called so because its bark was 
covered with seal-like impressions. They formed vertical rows 
or spirals and were circular and hexagonal, while the Lepidoden- 
dren tree had rhomboid and diamond shaped sears. Figure 13 





1. CALAMITES SUCKOVII FROM PRINCETON, KY. 


140 FLORA OF WESTERN KENTUCKY COALS 








represents such a Sigillaria bark. It was found on the coal 
slab in the North Diamond Mine of the St. Bernard Coal Com- 
pany near Harlington, Kentucky.. The outline of the scars 
appear in pyrite or iron sulfide on the black coal and make a 
very impressive fossil. In its branchings leaves and fructifica- 
tions the Sigillaria resembles closely the Lepidodendron. 

It is impossible to distinguish between the roots of Lepido- 
dendron and Sigillaria. When first discovered they received the 
generic name of Stigmaria and only one species, S. ficoides 
Brongn., has been established. The Stigmarias are cylindrical 
casts characterized by a smooth or irregularly wrinkled surface 
bearing spirally disposed circular scars bounded by a raised 
rim and containing a central pit. Figure 14 shows an impres- 
sion of S. ficoides from the Nicholson Mine at Henderson. The 
rootlets were attached to the small circular sears which sup- 
pled the tree with water. 

The Stigmarias are often found to be of considerable 
leneth, frequently from 20-30 feet. They seem to have spread 
in four directions from the tree basis and have forked repeat- 





16. ANNULARIA SPHENIPHYLLOIDES FROM BRAIDWOOD, ILL. 


PLANT GENERA OF WESTERN COAL FIELD 141 





edly. They run close to the surface of the ground upon which 
the tree stood and were admirably adapted to support high trees 
in a mud soil. 

The Lepidodendron and Sigillarias were spore bearing cryp- 
togamic trees nearly related to the club mosses of our time and 
formed with these the order of Lycopodiales. 

Another recent plant group, the Kquisitales or horse tails, 
were represented in the coal measures by gigantic tree forms. 
These ancient plants are now classified under the genus Cala- 
mites. <A good specimen was found northwest of Flat Rock, near 
Princeton, Kentucky, and is shown in Figure 15. Calamites 
had, like the modern Equisetum, a jointed stem with branches 
radiating above the nodes. It grew up to a height of about 
20-30 feet and was a swamp plant. The stem was born on an 
underground rhizome and was marked on the surface by longi- 
tudinal ridges and grooves. The leaves were attached to the 
branches in whorls or circles and were lanceolate or long and 
narrow. 

The leaves of Calamites are usually described under the 
generic name of Annularia. Figure 16 shows a good specimen 
of Annularia Sphennophyloides Zenk which was found at Braid- 
wood, Illinois. 





17. SPHENOPHYLLUM EMARGINATUM FROM WEST KENTUCKY 
SEEN EIN Ova7. 


142 FLORA OF WESTERN KENTUCKY COALS 








A completely extinct class of plants is represented by the 
genus Sphenophyllum. It has no living relatives. It seems to 
have been a water plant rooting in the bottom of ponds and 
ereeks and consisted of floating stems with whorls of wedge- 
shaped leaves. Sphenophyllum means in Greek a wedge-shaped 
leaf. Figure 17 shows Sph. emaginatum, Brong., which was 
collected in Mine No. 7 of the West Kentucky Coal Company 
near Sturgis, Kentucky. Another specimen of the same plant 
from Braidwood, Hlinois, is shown in Figure 18. Hach whorl 
of the plant contains leaves in a multiple of three. The leaves 
‘are finely teethed at their broad end and the larger ones are 
usually more or less deeply divided by a medium sht. The stem 
was noded like that of Calamites, but had no ridges. It con- 
tained a triangular center from which rows of woody fibers 





18. SPHENOPHYLLUM: EMARGINATUM FROM BRAIDWOOD, ILL. 


PLANT GENERA OF WESTERN COAL FIELD 143° 
radiated. A microphotograph of such a stem, cut out of an- 
Enelish coal ball, is shown in Figure 19. No living plant has a- 
similar arrangement of tissues. 

A great group of plants well represented in the vegetation’ 
of our time and very predominent in the Coal-Measures was 
that of the Ferns. Innumerable fossil ferns are known but few 
have been found until now in western Kentucky. The specimen: 
represented in Figure 20 was collected with many similar impres-. 
sions at the railroad crossing in Moorman, Kentucky, along the 
Livermore branch of the Louisville & Nashville Railroad. It 


. 





19. SPHENOPHYLLUM STEM IN TRANSVERSE SECTION FROM COAL 
BALL, 


belongs to the genus Neuropteris, but a more detailed determina- 
tion is difficult on account of the poor state of preservation of 
the specimen. It is perhaps the same species (Neuropteris: 


144 FLORA OF WESTERN KENTUCKY COALS 





rarinervis) aS represented in Figure 21 by a specimen found 
in Mine No. 1 at Spring Valley, Illinois. 

When we examine fossil fern leaves from the Pennsylvanian 
system we rarely know whether we have true ferns or seed 
ferns before us. The latter group is now extinct, but had formed 
in the past a link between spore plants and seed plants. The 
seed ferns had a fern habitus, that is they looked in most 
respects like regular ferns, mostly tree ferns, but they bore 
seeds on certain leaves. Such a seed is shown in Figure 22 





20. NEUROPTERIS LEAVES FROM MOORMAN, KY. 


which represents a specimen (Physostoma) from Spring Valley, 
Illinois. An excellent microphotograph of a fern seed is shown 
in Figure 23. It is a longitudinal section of a Lagenostoma 
seed taken from an Hneglish coal ball. These seed ferns are now 
classified by American botanists, with the Gymnosperms, under 
the group name of Cyeadofilicales, or Fern-Cyeads. In England 
they are called Pteridosperms, which is a Greek translation for 
seed ferns. 

The Cyecadofilicales lead us to the great plant order of 
Gymnosperms, which is also represented in the Coal-Measures. 
The only genus which was found in Kentucky is Cordaites. 
Figure 24 shows a slab covered with Cordaites leaves which 


PLANT GENERA OF WESTERN COAL FIELD 145 








was found in the West Kentucky Mine No. 7 near Sturgis. A 
species determination is impracticable because of inadequate 
preservation. 





21. NEUROPTERIS RARINERVIS FROM SPRING VALLEY, ILL. 


The above described groups characterize the flora of west- 
ern Kentucky durmeg Coal-Measure times. There were no 
flowering plants in existence at that time, nor palm trees. We 
know nothing about grasses and herbaceous plants because they 
did not lend themselves readily to fossilization. Only plants 
with deciduous leaves and with heavy woody stems could be 
preserved. It was a rather monotonous flora without bright 
colors. Green leaves and brown stems, possibly yellow spores, 


146 FLORA OF WESTERN KENTUCKY COALS 





were in abundance. But after all it was a vegetation following 
very much the same biological laws as exist today. There must 
have passed more than a hundred million years since the time 
when coal was laid down in the Kentueky-Illinois-Indiana basin. 





22. PHYSOSTOMA SEED FROM SPRING VALLEY, IDL, 


Vegetation has changed since in details, but not in its funda- 
mentals. How many hundreds of millions of years must have 
elapsed until the vegetation which we attempted to visualize 
in these lines had evolved cannot be fathomed by present day 
science, 


THE PRACTICAL VALUE OF PALEOBOTANY 


Naturally the question presents itself, what are the prac- 
tical applications of the examination of fossil plants, as found 


PLANT GENERA OF WESTERN COAL FIELD 147 








with coal? Their knowledge is helpful in determining the 
different coal seams. It is often doubtful what coal seam may be 
under observation and the coal prospector wants to be certain. 
Also in deep shafts a new seam is frequently reached and its 
nature may be doubtful. A thorough study of the various floras 
of Kentucky, Illinois and Indiana seams is in progress, and 
With it a revision of the coal geology of these States. 





23 IWAGHNOGSTOMA SHED IN LONGITUDINAL CUT FROM COAL 
BALL, 


A correlation of the seams in the great eastern basin of the 
Province of the Interior, the technical name of the coal field 
shared by the three States, should be helpful to the coal indus- 
try. At present the seams bear different numbers in the three 
States and often even in the same State they differ according to 
local ways of numbering. Hach seam has its peculiar qualities, 
in heating value, in ash content, in humidity, all of which are 
factors of industrial importance. There are, of course, varia- 
tions in the quality of coal even in the same seam. But entire 
seams were laid down under more or less uniform climatic, 
eeographic, and biological conditions, and therefore tend to 
be rather homogeneous in quality. The great task of correlating 
the coal seams of our basin is merely in its beginning, and it 
should be brought to a more accurate conclusion by more 


148 FLORA OF WESTERN KENTUCKY COALS 








a. CORDATT Hs! PROM WEST RINT UCKY MINE iO. 


research along these lines. A similar task has been accomplished 
for the coal basins of northern France, Great Britain and 
Upper Silesia. ° 

Manuscript completed October 30. 1922. 





Ve 


A 
BIBLIOGRAPHY OF THE MAMMOTH CAVE 
OF KENTUCKY 
(Ninty-six Titles) 


3y WinLArRD Rouse JILLSON 
State Geologist of Kentucky 


During the past two or three years a number of new caves and 
caverns have been discovered in the Mammoth Cave region of Edmon- 
son County, Kentucky. Several of these have been opened to the 
public by their owners, with the result that popular attention has been 
turned toward exploration of the caves of Kentucky as never before. 
A large percentage of the automobile tourists visiting or passing 
through Kentucky have come to plan cave trips en route. This class 
of visitors alone have increased annually by the thousands. This 
bibliography has been prepared and is now presented in response to a 
widespread and insistent demand for information as to the literature 
relative to the Mammoth Cave region. While there are literally hun- 
dreds of caves, large and small, in this karst section of Mississippian 
limestone in Southern-Central Kentucky, the following are the best 


known caverns. Popular names are given. 
Mammoth Cave, Great Onyx Cave, Colossal Cavern, Hidden River 


Cave, Horse Cave, Crystal Cave, New Entrance to Mammoth Cave, 
Ganter’s Cave, Dorsey Cave, Salts Cave, White’s Cave, Dixon Cave, 
Proctor Cave, Long Avenue Cave, Preston Cave, Highland Cave, Indian 
Cave, Parker Cave, Doyle’s Cave, Cave of the Hundred Domes, Mam- 
moth Onyx Cave, Diamond Cave, and Cedar Sink Cave. Each of these 
caves exhibits characteristics differing from the others and all are 
quite worth while the time of the sightseer and explorer. All of these 
caverns are closely adjacent to the Louisville & Nashville Railroad and 
the Dixie (automobile) Highway. 
ANONYMOUS. 
*A Description of the Mammoth Cave of Kentucky, the Niagara 
River and Falls, etc., 44 pp., J. M. Hewes & Co., Boston, Mass., 1850. 
*4 Guide Manual to the Mammoth Cave of Kentucky, 38 pp., Glas- 
gow Times, Glasgow, Ky., 1876. 
*Mammoth Cave. The New International Encyclopaedia. Second 
Edition, Vol. XIV, p. 746. Dodd, Mead & Co. 1920. 
ARNELL, DAVID REESE. 
*Meditations in the Mammoth Cave, Kentucky (a poem), pp. 42-49 
in Fruit of Western Life or Blanche and Other Poems. 216 pp. 
J. C. Riker, New York, 1847. 
BAILEY, G. S. 
Great Caverns of Kentucky; pp. 19-35 Church. Chicago. 1863. 








ralece Starred titles may be consulted in the private library of W. R. 
illson, 


150 BIBLIOGRAPHY OF MAMMOTH CAVE 





BINKERD, ADAM D. 
Pictorial Guide to the Mammoth Cave, Kentucky. A complete 
historic, descriptive and scientific account of the greatest subter- 
ranean wonder of the Western World. 112 pp., illus. Cincinnati, 
Press of G. P. Houston, 1888. 
The Mammoth Cave and Its Denizens; a complete descriptive 
guide. 3 pp., 1 illus. Cincinnati, R. Clarke & Co., printers, 1869. 


BIRD, ROBERT MONTGOMERY, 1806-1854. 
Peter Pilgrim: or a rambler’s recollections, 2 vols. Mammoth 
Cave, Ky. (in Vol. 2), Philadelphia, Lea & Blanchard, 1838. 

BURROUGHS, JOHN. 
Riverby; pp. 242-251. Houghton, Boston, 1894. 

CALL, RICHARD ELLSWORTH, 1856. 
The Mammoth Cave, Kentucky. A sketch published by the Mam- 
moth Cave estate. Louisville Courier-Journal Job Printing Co., 
189.2 (32 pry inel slus.- niap). 
Mammoth Cave, Kentucky. 12 pp., incl. illus., map. Louisville, 
Ky. Louisville & Nashville R. R, 1897 (?) (a reprint from the 
pages of the National Magazine published in Boston, Mass). 

COLLINS, LEWIS. ; 
Historical Sketches of Kentucky. 560 pp., 40 illus. Pub. Lewis 
Collins, Maysville, Ky., and J. A. and U. P. James, Cincinnati, 1850. 
Describes Mammoth Cave of Kentucky, pp. 157-158 and 254-261 
met. 

CROGHAN, JOHN. 
“Rambles in the Mammoth Cave During the Year 1844, by a visitor. 
101 pp., 6 pl., fold. map, by Stephen Bishop, Louisville, Kentucky, 
Morton & Griswold, 1845. 

DAVIDSON, ROBERT, 1808-1876. 
*An EHxeursion to the Mammoth Cave and the Barrens of Kentucky. 
With some notices of the early settlement of the state. 148 pnp., 
1 illus. A. T. Skillman & Son, Lexington, Ky., 1840. 

DAVIDSON, ROBERT, 1808-1876. 
An Hxeursion to the Mammoth Cave and the Barrens of Kentucky. 
With some notices of the early settlement of the state. 148 pp., 
1 illus. Thomas Cowperthwait & Co., 1840. 

DICKEY, MRS. FANNIE PORTER. 
*Blades o’ Bluegrass, contains Mammoth Cave and a part of The 
River in Mammoth Cave, poems by George D. Prentice, pp. 9-12. 
John P. Morton & Co., Louisville, Ky., 1892. 

FARNHAM, JOHN HAY, 1791(?)-1883. 
EHatract of a letter from John H. Farnham describing the Mam- 
moth Cave in Kentucky. (In American Antiquarian Society, Wor- 
cester, Mass. Archaeologia Americana. Transactions and Collec- 
tions. Worcester, 1820, vol. 1, pp. 355-361.) 


BIBLOGRAPHY OF MAMMOTH CAVE 151 





FLINT, JAMES. 
*Letters from America, W. & C. Tait, Edinburgh, also in as 
reprint Early Western Travels (1748-1846) by Reuben Gold 
Thwaites, vol. [X, letter XXI, pp. 281-282. Arthur H. Clark Co., 
Cleveland, 1904, describes the Mammoth Cave but does not name it. 


FORWOOD, WILLIAM STUMP, 1830-1892. 

An historical and descriptive narrative of the Mammoth Cave of * 
Kentucky. Including explanations of the causes concerned in its 
formation, its atmospheric conditions, its chemistry, geology, zool- 
ogy, ete. With full scientific details of the eyeless fishes. 225 pp., 
front., plates. Philadelphia, J. B. Lippincott & Co., 1870. 
*An historical and descriptive narrative of the Mammoth Cave of 
Kentucky. Including explanations of the causes concerned in its 
formation, its atmospheric condition, its chemistry, geology, zool- 
ogy, etc., with full scientific details of the eyeless fishes. Fourth 
eaition, 241. pp. front. 11 pk;-iold; map:. Philadelphia, -J. «B. 
Lippincott & Co., 1875. 


GAUSE HARRY TAYLOR, 1853. 
A detailed description of the scenes and incidents connected with 
a trip through the mountains and parks of Colorado, as accom- 
plished by H. B. B. Stapler and Harry T. Gause, July 21-August 
20, 1871. 205 pp. (Cover-title: Colorado, the Rocky Mountains, 
and the Mammoth Cave (by) Gause.) 


GRATZ, HYMAN (reputed author) 
Green River or Mammoth Cave. Medical Repository, vol. 17, 
1814, Philadelphia. First description of Mammoth Cave as a nat- 
ural wonder. Map by Rafenisque. Vol. 18 same contains letter 
descriptive of mummy found in Mammoth Cave. 


HOVEY, HORACE CARTER, 1833. 
Celebrated American caverns, especially Mammoth, Wyandot, and 
Luray. Together with historical, scientific, and descriptive notices 
of caves and grottoes in other lands. 228 pp., front., illus. plates. 
Cincinnati, R. Clarke & Co., 1882. 
Guide Book to the Mammoth Cave of Kentucky; historical, scien- 
tific, and descriptive. 75 pp., fold. map, illus., 6 pl., 13th ed. rev. 
and enl. Cincinnati, R. Clarke & Co, 1891. (1882). 
Guide Book to the Mammoth Cave of Kentucky; historical, scien- 
tific, and descriptive. 75 p., front., illus., plates, maps (1 fold), 
14th ed., rev. and enl. Cincinnati, R. Clarke & Co., 1891. 
*Mammoth Cave of Kentucky; an illustrated manual, by the Author; 
assisted by Richard Ellsworth Call. With historical notes, scenic 
accounts and descriptive and scientific matters of interest to 
visitors, based upon new and original explorations. Louisville, 
A fel a Morton & Company, 1897. 


4 


152 BIBLIOGRAPHY OF MAMMOTH CAVE 








HOVEY, HORACE CARTER, 1838. 
*Hovey's handbook of the Mammoth Cave of Kentucky: a practical 
guide to the regulation routes, with maps and illustrations, 63 pp., 
incl. 17 illus., 5 maps. Louisville, Kentucky, J. P. Morton & Com- 
pany. 1909. 
Mammoth Cave of Kentucky (Hovey and R. E. Call); with an ac- 
count of colossal cavern. Rev. ed. By Horace Carter Hovey. With 
historical notes. Scenic accounts. Descriptive and scientific mat- 
ters of interest to visitors, based upon new and original explora- 
tions. Louisville, J. P. Morton & Company, incorporated (1912). 
L3i- pp. 
Mammoth Cave. The Encyclopaedia Britannica, eleventh edition, 
VOloc\ LL DiD ol ooo,n With Deo ele 

JAMES, G. W. 
Our American Wonderlands,; pp. 272-282. McClurg, Chicago, 1915. 

JOHNSON, CLIFTON. 
What to See in America; pp. 219-20. Macmillan, New York, 1919. 

JOHNSTON, C. W. 
Sunny South and Its People; pp. 89-94. Rand, McNally, Chicago, 
1918. 

JOHNSTON, FRANCES BENJAMIN, 1864. 
Mammoth Cave by flashlight. With 25 illustrations from Miles 
Johnston’s own photographs. 59 pp. Washington, D. C. Gibson 
Brothers, printers, 1893. 

JONES, WILLIAM BASIL. 
Wonderful curiosity; or a Correct Narrative of the Celebrated 
Mammoth Cave of Kentucky; with incidents and anecodtes. 67 
pp. Russellville, Kentucky, Smith & Rhea, printers, 1844. 

KING, MOSES. 
Ed. King’s Handbook of the United States; pp. 276-77. Matthews, 
Buffalo, 1896. 

LLOYD, JOHN URI. 
Etidorhpa, or The End of the Earth, pp. 88-104. The Robert Clark 
Co., Cincinnati, Ohio, 1896. 

LEE, EDMUND F. (C. E.) 
Notes on the Mammoth Cave, with a map. 1835. 


MARTIN, HORACE. 
Pictorial Guide to the Mammoth Cave, Kentucky. 116 p. Illustrat- 
ed by S. Wallen, Jno. Andrew, J. W. Orr, and N. Orr. New York, 
Stringer & Townsend (1851). 

MILLER, ARTHUR McQUISTON. 
*The Geology of Kentucky. Series V, Bull. II. Dept. of Geology and 
Forestry of Kentucky. 1919. Description and Geology of the Cave. 
References. 


BIBLOGRAPHY OF MAMMOTH CAVE 153 


MORRIS, CHARLES, and LEIGH, O. H. G. 
With the World's Great Travellers; pp. 83-94. In Mammoth Cave. 
(Longworth, M. T.) Union Book Co., Chicago, 1901. 


MUNSELL, LUKE. 
A Map of the State of Kentucky. 1818. Locates and names Mam- 
moth Cave. 
Kentucky, reduced from Doct. Luke Munsell’s (Large map of 1818). 
1835. Locates Mammoth Cave. 


MURRAY, A. M. 
Letters from the United States, Cuba and Canada; pp 319-323. Put- 
nam, New York, 1856. 


NELSON, NELS CHRISTIAN. 
Contributions to the Archaeology of Mammoth Cave and Vicinity, 
Kentucky. 73 p. incl. illus., plates. (Anthropological papers of the 
American museum of natural history, vol. xxii, pt. 1) New York. 
The Trustees, 1917. 


PACKARD, ALPHEUS SPRING, 1839-1905. 
The Mammoth Cave and its inhabitants, or Descriptions of the 
fishes, insects and crustaceans found in the cave; with figures of 
the various species, and an account of their allied forms, compris- 
ing notes upon their structure, development and habits, with re- 
marks upon subterranean life in general. Assisted by F. W. Put- 
nam. 62 p. (Annual Report of the Peabody Academy of Science 
for 1871). Salem, Mass., Naturalists’ Agency, 1872. 

PETERSON, C. J. 
Two Days in Mammoth Cave. (Extract from Peterson’s Magazine, 
1852.) Philadelphia and New York. 

POPHAM, WILLIAM LEE, 1885. 
Mammoth Cave Romance. 110 p. incl. pl. Louisville, Ky. The 
World Supply Company. 

PRENTICE, GEORGE D. 
*Mammoth Cave (a poem) in vol. ii., p. 557, 58, 59, A History of 
Kentucky by Lewis Collins and Richard H. Collins. Pub. by 
Collins & Co., Covington, Ky., 1882. 
*The Poems of George D. Prentice (edited by Piatt, John James) 
contains, The River in the Mammoth Cave and Mammoth Cave. 
Robert Clarke & Co., Cincinnati, 1876. 

PUTNAM, FREDERICK WARD, 1839. 
Remarks on the Mammoth Cave and some of its animals. Meeting 
of the Essex Institute, Salem, November 25, 1874, pp. 191-200 (From 
the Bulletin of the Essex Institute, vol. vi, No. 12, 1874). Salem, 
Mass., Salem Press, 1874. 

ROGERS, CARLTON H. 
Incidents of travel in the southern states and Cuba. With a de- 
scription of the Mammoth Cave. 320 p. New York, R. Craighead, 
printer, 1862. 


154 BIBLIOGRAPHY OF MAMMOTH CAVE 





SCHAUFFLER, R. H. 
Romantic America; pp. 99-133. Century, New York, 1913. 

SHALER, NATHANIEL SOUTHGATE. 
*On the Antiquity of the Caverns and Cavern Life of the Ohio Val- 
ley. Memoirs of the Kentucky Geological Survey, vol. 1, pl. 13, 
University Press, Cambridge, 1876. 
*4 General Account of the Commonwealth of Kentucky. pp. 26-27. 
John Wilson and Son, Cambridge. 1876. 
*4A General Account of the Commonwealth of Kentucky. Part XL., 
vol. II., series II., Kentucky Geological Survey, pp. 26-27, 1877. 


TAYLOR, BAYARD. 
*The Mammoth Cave, parts L, IK, and lis pp. 2180:225 eee 
(frontispiece) in At Home and Abroad, 500 pp. G. P. Putnam, New 
York, 1860. 


THOMPSON, JOHN, 1874. 
Mammoth Cave, Kentucky. An historical sketch containing a brief 
description of some of the principal places of interest in the cave. 
Also a short description of Colossal Cavern. 48 pp. Louisville Cour- 
ier-Journal Job Print., 1909. 

. TURNER, JAMES WILLIAM, 1848. 
*Wonders of the Great Mammoth Cave of Kentucky. Containing 
thorough and accurate historical and descriptive sketches of this 
marvelous underground world, with a chapter on the geology of 
cave formation. 116 p. Carrier Mills, Ill. Turner Publishing Com- 
pany, 1912. 

WARD, DR. NAHUM. 
Pian and Description of the Great and Wonderful Cave in Ken- 
tucky. 1816. 

WARREN COUNTY (KY.) RECORDS. 
Deed of Mammoth Cave Tract. Flatt to McLean, deed book No. 6, 
p. 49, Bowling Green, Ky., 1812. 

WILLIS, NATHANIEL PARKER, 1806-1867. 
Health Trip to the Tropics. 421 pp. (No. 3, Mammoth Cave, Ky.) 
New York, C. Scribner, 1853. 

WRIGHT, CHARLES W. 
A Guide Manual to the Mammoth Cave of Kentucky. 61 pp. Louis- 
ville, Ky. Bradley & Gilbert, 1860. 


*The Mammoth Cave, Kentucky. 68 pp. Harvey, Mason & Co., Vin- 
cennes, Ind. 1858. 


BIBLIOGRAPHY OF MAMMOTH CAVE 155 


MAGAZINE ARTICLES: 

5 American Naturalist 5; 739-61. (Dec. 1871.) Mammoth Cave and 
its inhabitants. Peabody Academy of Science. Salem, Mass. 
American Naturalist 31: 377-92. May 1897) Notes on the flora and 
fauna of Mammoth Cave of Kentucky. (R. E. Call.) Edwards & 
Docker Co., Philadelphia. 

Bulletin of the Pan American Union 41: 378-92. (Sept. 1915.) Great- 
est cavern in the world. Ar. 1-6. Washington, D. C. 

Century 33: 643-59. (March 1898.) Mammoth Cave of Kentucky. 
(J... Procter )x 

Chambers Journal 7th series 3: 782-4. (Nov. 8, 1913.) Visit to Mam- 
moth Cave. (Not in library.) 

Eclectic Magazine 21: 474-84. (Dec. 1850.) Visit to the Mammoth 
Cave of Keniucky. New York. 

Eclectic Magazine 53: 45-52. (May 1861.) Alammoth Cave of Ken- 
LUCK... NCW York: 

Journal of Geography 11: 386-41. (June 1913.) Description of 
Mammoth Cave. (R. H. Whitbeck.) 

Living Age 28: 125-32. (Jan. 18, 1851.) Visit. to the Mammoth 
Cave of Kentucky. E. Littell and Co. Boston. 

Living Age 92: 34-45. (Jan. 5, 1867. Down the Ohio to the uncer- 
world. Littell-and Gay. Boston. 

Nation 67: 145-7. (Aug. 25, 1898.) Mammoth Cave and Cloudland. 
Ghisel san INnGk<) 

National Magaine 7: 204-13. (Dec. 1897.) Mammoth Cave of Ken- 
Pichi (CH -E. Calle) 


National Magazine 41: 821-39. (Feb. 1915.) Description of Mam- ~ 


moth Cave. (G. W. James.) 

Out West n. s. 8: 307-19. (Dec. 1914.) Description of Mammoth 
Cave. (G. W. James.) 

Science 21: 189-90. (April 7, 1893.) Mammoth Cave in March. 
(H. C. Hovey.) 

Scientific American 89: 147. (Aug. 29, 1803.) Balloon measurement 
of height. (H. C. Hovey.) 

Scientific American 100: 388. (May 22, 1909.) Kaemper’s Discover- 
ies in the Mammoth Cave. (H. C. Hovey.) 

Scientific American 116: 59. (Jan. 13, 1917.) Hlectric Lights in 
Mammoth Cave. Munn & Co., New York. 

Scientific American Supplement 60: 24680-1. (July 8, 1905.) 
Strange Mazes and Chasms of Mammoth Cave. (H. C. Hovey.) 
Scientific American Supplement 64: 125. (Aug. 24. 1907.) Mam- 
moth Cave Cathedral. (H. C..Hovey.) 

Scientific American Supplement 83:275. (May 5, 1917.) Archae- 
ology of Mammoth Cave and Vicinity. (N. C. Nelson.) 

Scribner’s Monthly 20: 914-925. (Oct. 1, 1880.) One Hundred Miles 
in Mammoth Cave. New York. 


156 BIBLIOGRAPHY OF MAMMOTH CAVE 


PAMPHLETS: 
American Museum Journal 17: No. 4, p. 221-233. (April, 1917.) 
Kentucky and Her Cave Men. (N. C. Nelson.) 
Louisville and Nashville Railway Subterranean Wonders. 
Louisville and Nashville Railroad. Swmmer Outings, p. 9. 1916. 
Kentucky Motorist. (March, 1917.) pp. 17-19, 20. Seeing Kentucky 
and the Mammoth Cave. (H. F. Randolph.) 
Kentucky Motorist. July, 1917; pp. 7-8, 14. Day Underground. 
(Helen Randolph.) Louisville Automobile Club, Louisville, Ky. 


Kentucky Motorist. Dec. 1919; pp. 6-7. All Highways Lead to Ken- 
tucky's Wonderland. (Helen Randolph.) Louisville Automobile 
Club, Louisville, Ky. ) 


GOVERNMENT DOCUMENTS: 


U. 8. Congress. Military Affairs Committee, House. Mammoth 
Cave National Prak Hearing (Feb. 1 and 5, 1912.) on H. 1666, es- 
tablishing Mammoth Cave National Park. 

U. S. National Museum. Proceedings. 1903. v. 25, pp. 223-236, 
Observations on Crustacean Fauna of Region about Mammoth 
Cave, KY, 


NEWSPAPER ARTICLES: 


Louisville Courier-Journal, Jan. 28, 1912; sec. 4, p. 1. Mammoth 
Cave and the Proposed National Park. (E. C. Logan.) 


Louisville Courier-Journal, Sept. 10, 1916, sec. 4, p. 1. Along Dixie 
Highway; the Country of a Hundred Caves. (Tom Wallace.) 


Manuscript completed Jan. 10, 1923. 


a 
iv \ 
ee 


INDEX 


A. 
Page 
ge sg 0G ES BS se Rea ei cay San ee 128 
OOS CO OR te aS aT ha eg Dias ate Aan ear ane SA ee Aer ere a enna 9,109 
eT CCITRI TC Tari eee ee ek ihe ec eA easel a Ac 108 
Sees a eee Vt SOUIN IN LUA EL ISUOL Vr sere ccrecis es eret nc nenstebine ficacdenskovacedecn 107 
TW SCEEL "ta RG = a eel ae an SOE ee a ee et Cen eR 2 Ra 42 
SEES OUTST poe § © See A a9 cease ar ey Sa SE Sk Se etree ne a nee Ne hi 20 
So UO LEE aa BE FA a ie om BeBe, Fi 4 Onn hota aeal apres ae: 51 
(Ge UIE ER NS a ne Aa oe a OR he ea 101 
eRe LER ET) RS ee re cg AEE E AIG No Pee cay eke, aaah Fh eck tet Get wagot ca eeeietets 122 
Bete esta ATIC EOC eae rei ciret er ccepe ees Mt one oeh ee”, oun ot Wusyete Mew iecoas 31 

B. 
(2 USES Res ae ie ee A a Re PE tis 
Prem TTA ONT) TAG, VP er, en ee os cad cena gcnnt- basnsanvussouasendecus wacesaaveen 109 
err Tem C TULL CIV tu see oe Cer re ae aay 98 
LEP CAIMIR GLA A TUTE BS OS Te San FT Tae ote Poe ne OR Sees 2 ies ea 81 
ROSE ATG CUT AYE al we arvensis 32, 34, 39, 42, 50 
COS TEM ON gas BAAS pte Al ce Ua ink oe 2 ay pr a a 107 
ESR Gad Bat DT dag ee eR enh ced er ee Pt ae a 53 
VSG RECS STS EUSapeatee! ir SF WC a ah le a oe A Pe = 116 
ON es trate Cre Vi eM ee ce eas I ig ca Vaapren ctidbi ance ee oscdes 108 
PA CaVR SG 8 BAYES gy nt SOIR 1 0 yh 2 Ni oy ar dD DE ea ais Gy 
SUPINE pe cere oR as a0 RO ee EO PC ey 120 
PRE CEU UD TT 1s eS Voge eee cee ee a oe eel et eee wales 107 
She. pega Sa Wg OE yo a AN a ae ane eek ha 2h Ser ena ee ae 108 
DENP 20 Ss Nig CEP of OUR ON I care ane es ee icone ae RE Seca 43,-50,.51;.61;.63, 67 
Ieee ESTES CLC LUT EC Inv ee ee ee od Se he ies ee 8 80, 98 
Sete VV LU Ta GT CC LOY ao0 2) ccc, cece cies each Rie etre canted gies kee LB 
atts, “CUAS. .....22 Ao ar Co RE Oe ee psa t ie Be A 9, 40, 44, 50, 60, 61, 118 

C. 
ee reMs LDMMRRC LEDC nee, cS. So) Soh ects cre oe tiee E RLT trae), ct mE 1, 39, 43, 44 
ETI Se TED COWES A 19 0 oe eee aie ae re a Ee RE SE Ac ra Regt RENE A 89 
heat) Lalys oD) Ya Es a W01 RY ee SAR NR aE Sg ae gh ee nee Man 107 
JD ECU AMEN GL pint ARI Nene SOAR, ni tt Oe SA a, (a 101 
CGT CUBMILIT ope techs 8 LIES ST Hal ee eee Aa a A ee Sea 2,19, 46 
Seay eres Shae Ome WC] 1G: AC eos aoe doen ans op sn wacde densest esceect siniaceseccnee 5 
ENE TSR R CR TE Sab iy py BE te aaa ee ees Oe Eee Za, a0 
TS TUNE ge OES PEND Ey 0 ip oe a a a a 8 


(MeStel Fauna s. <2 4e7-ci. eee Ie eter sckars seceeonts Fania Veeeevis to naacte sewed 3, 38 


158 INDEX 





Page 
Chestér= Series #e-2. See SAMEEREN: Mey Pat Riek PL ee RE Ry, 31, 34, 39, 40 
Ghristiany Gout ye ares oon cee et eee ey oG pee eee 43, 44, 50 
Cinein nati wes ere See ces ek ee ea 0 ee ee ee LS 
Gineimnati. “A rehearse  o 115 
CV Wat ee ie er ara ch code snd ee ce ee LYE 
Gla xton ie ee oe a es ee 1,2, 3;-31,.55, 59, 66) (996i Soe 
Clayalitke ROadmere ect skeen eee oe terre eae 48 
Wlitvord to VOU Ns 6pie se ee a ee as ee ee 107 
CGE COT SG OUT Ei sere oa es ag ah oe ee eee sinh: 
ClOT OS ORI ATLOUS roo con so ek ee 2 ee 83, 91 
ClOT@RDIMESTOTIC 2. Sigckcntse occ cde ee nae ee cen tee ee $1 
Coal]Plants: GGnerai pec. sce eae eck eee eee re Lag 
COx bene be wae cs ns wanes Gnade slcca¥e sitecds iw acide iacdiegone = Ge tee ae eae cele: Cae ea 3 
Grider. 235.55 her a ee ee 25 3,20, 29, VO noe 
Crittenden. Coun ty~ Skea: seee tacos rete na ae ee ee ee 43 
COULT) ARR WL She ce eee Soca ee Bac ee So aco el SA ack Cece ee ee 120 
Cumberland: »HsCarpmienee 5 see se ooscc-c oe eee ie 20 
CUMLDETIAT G1 VC ie ee tes eae cee ee ee eee 2, 109 
CY DPeSSADATLOSLONC eet canton re ieee eae rere ek ee oe ee 39, 40; DE 119 
DD 
Davis > J SEMOrton Setecck lise aes, ee ee iis 
DAawsOn= Springs. het eects Ale ee 55D 
DeToniaweoandslone) Bee Awe ee ee ee 83, 87 
Devonian tilsimestone™ -:..2b) cate. Sees ee ea 2 
Dodgee,evictoreK . = niki Shc ee 113 
Donaldson’ At Bae Bs a a eee 2 
DTUry; HOM Ge ate Ratt cho eee A pee ee 133 
Dry? ‘Creek 3s. Teere a ri a | ere ee coe ses er eae ate oy eee ane ce LT 
DOr any a ees et ee A a ee ene eee 2 
, E. 
1 DET) weed Ball Fe (5s Pee ape hae CE see eet g eB 110 
HWasternuKentucky Goal field...) 6 ee ee es 115, 126 
FEO Dy Cree ere ee oes waren ee ee oe nee 2y Bet 
Hine lemMan nh: 2 ee ee ee ae wo nes ee eet cate oe eee ape 
Liles 
Wairview © Mine aera eee a ene tee oe Re tee 43 
WATMCTSVING reel oc See cope eee ca kn ca, 24 o> OD 
Farmersville’: Dome © iiss ee ee ee 101 
NWarmersvilles Log of¢ wells ats ie ee ee 102 
Wie Cee ROCK wei ae cee le ee ee is | er 22, 68, 19; 101 
bd hg itt Reemerene nine ee otis 7, rant. ene Mey PRO RIM Pm EN Re eS Ake be 2 
Flynn: Creek. 23215: ee ee ee et ree 18 
Hredonias-“LimestOne@nies. iis aes ee ee 28 


HIN KNOUSED eT WV ees eee eee RM Dh Con cre wl oeteb e yA a NE OE Lis 


INDEX 159 





G. Page 
ELST TOM BAG UWe 07 1h Pee oa ei cena mei To A ae ale irra 2: a ee Oe 50 
joe alee FIRS Sat I Se Se OR gt... ieee Sk Se Oh eRe de, ot - iine 89 
ed ay Ta Mee a i a PO ea PE OS 67 
CI Se TOR 8 ee See Sf En ee en la) na Me aes 66 
Rupee FEMMES CPE TYI LCT TY ed bs aniston ceed oP CRORES sleds wind Albay as 62 
ear Sere i werb ceQersp Rapa te Re te ee yap ea teen a 18 SA ne Cir 0s 63 
We Oa 1aMG Sd Re eae | oo Cig Ane 5 ie oe re a ener 58, 59 
SCRE 6 Na ee Se ee ee a eS eee Olde, Oe 
Fue IRS ay a Ee BG oie: a A, SoA: 
He 
DP MRILO UMUC Cet 2 Sehr Ge ten, gee ee Ae Ue oN a Ce ype 
Pome Te GOUNT Ye LIINOIS cul os ecco cece ee 9, 18, 32, 34, 38, 39, 42, 74 
ERE INTL TS 2 a bee ee coc aa |) 2 A See SI Ye ht ase ike ee 67 
RRR DIOTU ee COPIA CEO: Gaette os tr ee eee ae Se a et oe ee 61, 63 
MEPerTU TT 2 SATS LONG se meee e. ..es tr, eee eee 61 
OR Ch tea 1) meVY Tiedt VON Yam se es Soe oo S.-oa oeeec eeepc ov Rea aee 107 
Sr eeeee CS 1110 iy a eee ie er Be ce Pebe ooh cen eens wu sesno minis eet ab 4 
(a Seytatiete 0 ibd 2a 2% Snes Sos er a a ce I 109, 110 
EEE UAB O  OC) ee me 3 se ea SS aeanie wandered dete osclcaehy chs halons dts 61 
cid eR ESS ol BIW eg iS 02S SE ee oe So) AY ee Se Am as: 
Merrureroemea TC) IV SMe eat yemess em ee eee oo 5 fh occ ea sas cntecicses qaunnyssedanuweueeWbetevs ceees 109 
CAE WOR ALC yale GS Sa oo 28 oe gel Ee 2 eee pee eo As ae oe Se 109 
eT ST EN eto Ee of S|, a 2 EE ae he EP, JE Se es rae 44 
OS PTD ESS AS Bed BF Sgt GEES ye ey Ee a 2 See ee ek Ge a 102 
Te 
og Rg TST ERO (04 Spey eI ok aaa dre a ee Mf 
LSTA D SSE CSS SS Ea espe ie Ve al ip a a Ba Re ne ee lh lero 53 
LUNTEN Sap eS es SRST cesar ee 14 
EMER EST | CUM: cre Geiss, 2M ee ee Be os okt ed rote) Seen 13 
Af 
SP URRMLS 5() MN pty We. Cee ee ee A LL” Since, Sa tae 122 
ree OULIN Vaehllcat) to ieee ee ee ee eee es 83, 85 
SIR Tote \ GS ane = TARR tid olla eae Mice cep NE Bead Sea a Pe 20 
OL Sea 25 Bh RII ie PR aie A ag A A 44 
EERO OUEST IME MYO) 601s 5: gan Jie Siena eae BES 21) eee arene ae mE 107 
SU OMT 7 CECE Big OC oe ae ee SR i A Ede a A St 9 
Dea ea OES SC tect eRe enc 8 2ee.- O Seard te wieght ae Se 133 
Me OPTL ETI CEASA) UT) Veet ee toot ee ee ec I a We ns a eneteeee 108 
TOURED ESOT N UD 703 a0 eh -ZaeS oke Sin «8A eae Ba tes ere SO ta a 116 
ese TT MeV V com Fu mr eee ec eres, el Ih eee es oe ae ae orld dg lool ta 


rIETTCET EM CONT i toy eee Lt ce os eee ee oS es, oh een Seer 73 


160 INDEX 





KS Page 
Kentucky (Geological  Surveye ee sens oe pier oe ee S 
FO THK ST SA TLD 2 a Sev reciecs eee ee tas eae ant ated tet tarts aces oceans ee 87 
Mlwkal@a TimMestOne eens ee ee ee ee 82-85, 90 
KN OUE Woe eee cee a ee Pee Se echo ee Livi 
L. 
Watavette -Gravel) 5.2) ee, nee ee ee Se cee 93 
Tyan DS Cree ia cee ant es ee es ee 61, 63, 66 
TAM DIOP WY Tee reece aac we ee oe ee ee 97 
TISSCUCT UR ts CO sree eee 2 Coro tree cacao ene Ge are ae 127,128 
FSO WAS UO W Thies ect ner cccka cea h ce Res aes ed ee ele tt ene aan 2, 66, 85 
TOIT CV RW oe MR ea os conse re ae ee Se 1177426 
ToithOSUr GEL OT) Rees 5 ae eS ety ata ee eee ee cee oe aly; 
Livan Stone cCOun Uy ae ee ee ee ee ee 32, 43, 44, 46, 54, 62, 74, 86 
Lone AUN COrs 2 ce stores Rea ee tea in ee ots eee 109 
TiO Were Ova Rg oe en sr ee, 25 
TIO WEEY, Willian ee ee BPMs Ne hs peer Ee A 8 113 
M. 
MIB ENOL AY eco eer vd Asse oe ee et ee 122 
Mammoth Cave \..5 55 iesecce ee ee ce ee 120, 149 
INV EP LON sce ee ech ss ooe ee Fee ods ah ee 43 
MaZON ss Greek evi sei eee au se esha ew hg ee ta Te re en ee 133 
MECC Mri ed Wo ao sree tee eee ee 113 
MGM AT IAT SA YO s.r, ete naar eee ee ee 3 
MCGO Watt re oo. a Re ee aso 
McGowaneStation se roe i Occhi cee eee ee een eee ot 
MCA 0 Was ree Ke rrae Fo cscaecstecteet a boc) BE caaena eee i ena, cae 110 
ju C2) FB gfe Cao OF: AY Bi: Roe Sue eee Penee ap et en omer chard, SO tenet 4 OR Enpiaee: aoe 78 
Menard , UBiestone se iets .c ct. betes oe. ceca whet eee ee, eee 43, 76 
Mill AS Drin ese ito cscerc cert ores cece the ee ee er ee ee 109 
MilleraxA rthurtMcQuiston test conics tee cec nt eee en ee 107, 117, 124 
MUIssissippl = RIV Gr ee oem cass i ecec ne cea ease eee ee 31, 43, 82 
MISSISSIPD Le V ALLOY om ee Ea ee enor ea ep eee 22,95 
MUISSISSIPDIA TESS CLiGS “ee ceee are cee recast tee ee eect eee ee 9 
IMEISSOUT Le Aerie errs oe ee cere la 2 19 
Mitchell ye Jes Kieren aes ee ee eo ae ee eee 173 
Monroe Couney cL ie. rae rete ite core yet epheat ee oe ee 31, 34, 39, 43 
Moorman ty Ke Ve er race eee oeeeee ee ee ene eee 143 
Morefields Shale rer picnics cutee nee eae tee eure erie th cvcen ence een ee eon aie eee 51 
MorgzannteldtCoaled- Coke® C0. sr ee ertesc eee ee ee 133 
MILO S VAT] ergo en tease nares ce caren aetna do ison iecr tet er ee 117, 120 
N. 
Nelsons; Noi. Cech ho os ire ce a ee i ee ee ee 109 


INDEX 161 








O. Page 
OL UTTER EES OPT ay Beles) ANSP ls Se i Bey Rie ein Pee He ae 5) 
OU ge Sule SS RN dep SI nee eae gue Re Rr or ce ey oe 53, 99,115 
CRIES Cet 0! SA UAE pt Rp IP et eS ER ped Ba 42 
CUNO ATE RG © Stk SS pee ais Dri No, AME Se anole ae Se ee teen e ae 19, 22, 95 
Se MMMCUNIETRESCRUICRT! Gordy ke? on oe Cae a ye ee eb exces ebwetraie DT, OL 
ye Teati BP se CSI a os Sones ui ape. AO pap a cs or, ot. 00 
Coy lg TR CALS 0 1a i ieee) EL Tl Se ET A eee ie ERs RR lo 14 
aan oe mM RTI) 2 Crete cour eka Met eek Boat «oes eyhnes Save denieuacaves eee eee 67 
wo nao. TRUS SPD et eae cy lis Na SiR te ee, Se ee a A ee SE er a 19 
es ae I aie SLT oe aay con as cal da dess Hecbasdestteiacsbow ie ees 20 

Ace 
MNT MRM CSCS Meee Maes 5. Brae pee pa os ao apa bo weghtee vant cea nhacpenns lated 34, 42, 45, 46 
ol ESTATES BB 1 CTSSSH COD Ye Peale ae ee eo OU Ree oe de ae dag 43 
ere Ce clay FOU USN en coer ht eed psec ee ee ee 48,51 
aC erereet YC ATCT SE OITGs tee oe eee ee eee ay ee ay a 
RCO, Bees A 2 a at | ee Fase ie PP 82 
mE es ean er TE Tcd le eee eee ey ee eee ed eae ls 87 
ENE EL TERED Teta VC IT) Ware tetace cise cel Soo o2ctcosecnacsacha> aces csc cbecadcexstemeeccsasecdaone 89 
cFoy tu TRS LAPP Gh GoW) aloo oh CO i oan a he See Re 116 
ae CEN GE CHEST CE ery eg et Pe eR od 2a Fo Ah a esac cadsent betene nam bye bts 
2 DSRS IGN Dna aca ge nt 43 
reo Oli mee ree her i, oS yee ee 108 
LOE) CEG CrP Co al IR EP AE ie Pe ny ee ss 8 90 
118 950 OES, Bg a Re Ry ee hte» aR ® Tre eS OTe Le eh eat Dee ee 85, 87, 90 
EL ON PESMD ECO i erent se ie Soren etch) uct nee ae See tee cae 89 
LTV UUES SSYSiy AU CONED gS Ape Sai ae on AEE aN at boat eA ToLO) 
eh Nil GI 09) le 2s le oi cn le a 280 a RD aie ee ee 110 
[2S TELE We 3 5 pe AE Taal, 22,522.00 56290 R00 
Princeton Guadrangie .200 5... Ll Oc lee2, ols 047 44, 47490100 
OME LOSES aac) SW Cem OTS Mad Te fae Ca he 0 Peat aes ie ace oa se 62 
Pee ee PCE NaGl WW! BSCO Wt) PLCORE eeceeces ee ee eet es a es ere oe 64 
SMMC CLemeraATINCrSViilGs FOG ode tc legs. ts rodeeese bes saad ta tee cea 68 

Q. 

Lue 
Premrrermra Ss Le CRCH LIST Vo Ed Lene cee eis fet ee ee ae Gy, it Se 43,77 
(So StS PEI SO LONE Ro se Se al Coe IPERS eee Re PES OS Ae I ODF oleoS 
Prete Isl INCStONG 22s 82 pcan ceect eee Se oe A Dole oe Sek Peat oh SAR 31, 34 
eaerrarar eared ome rd TTY eee oo Fes ee a ee oe oe ge ee los 
POSTS, SE gi eee salen SR Ae ORCA el. <r eS Ean A? Meee eRe On SEO aE 122 
ere en cme homie er oeee a aet e Bee OP IS A ee te ee 43, 45 
Reeartat pea SOL Ceres fons go eet et aa A ee 25 
UTES 2 8 lei gd ate Be ERE AL ENED eo I a ORR aE RT Sere a ae ee 2 
eee LW, ree Sen ee ee iat ae ys dP ek ee 110 


Pree OT ety Oi) Gmette se ne 26S oe ee eee)! 116 


162 INDEX 








Ss. Page 
malenin MAIMeCSTONG 5 cn rete ene a peu et ace cag ot eon ad re ee ee ee Ls 
SAIC PelLlG-ser es ee ec ee Se eee epee en: ee 107 
Sample “SandSton docs a tecee eee scat, oe eae seperated ae ee 43,50 
Sard ick. ROG botnet eos, ce ene nema Fat: 2 os eee 48, 62 
DAY COl Mie ee eee eee eee OF heen ae CREE On cay Loe ee 2, 94 
SCOULLS DUT 2 preter cc fonte ees ade ae ag ere cea 2, 31, 42, 44, 57, 58, 62, 100 
ALOT No De oe repre eso fat oeee es det Sacco ea ee ee Wa ee eae LG, 
SharoneConzlomerate . 2 eee pane toe erento 2 91 
SHOLErvViILl SSMEO UD Or eres insect ccsel hace ooeeenaes eee eee ee Berge o BY et 
SOG Y,.. Pie] ATG pisces eine oe ooh ae coe cance 0 ce ee ee ee ee 1B 
southern= Kentucky ~Cave.7 kee eee 109 
Southland = Coe eC OF eee 5 aesa sa bsce syne rawng acces eee ne ee 133 
spergen™ Limestone heise. ce aoe nccs cee ene 13 
SDP Creel hc Ce ee ee ee, ee ne eee 133 
StvGiair., OOUNtY 211i) ee hace ee 49 
St. Geneviev es limestones 27k ee ee ee 22; 38,090; 48 
St: Louis Vb Mest oneness ine ee nek Beet td di dotned ete eee 16 
St. Genevieve Limestone Fauna (Fredonia) ............2..022..222222-------- 29 
Structural Geog ye os er eee 99 — 
SULPNUrer Grech: -_ ni a Sea ee ee 58 

oe 
TAS Wp Bs Bo 5, os og ee ese ee ths 
PaaS PEIN Ses & che ok. Lh eee, ee Ie) a ae enn ee 53, 65 
Tara sSprin ese MOLMatiOn ® v.ccctcce-ctee -a toa reeeee ee ae Pe 63 
Bat SS DPINSSeoan USLOUM CS wie sec oe eee. eee to case cnka ate a eee 275 Gt 
PEnNGSSCO ses woes oe ene Re Pi ene NERS eT eae A 19; 20520 
‘Odd, COUNT VeIGy Oe i r= rt. ee eer ee eS eee 43 
TrAdewactery MOLrMatiOn stoke ee eee eet Se, oo veaeee eee 89 
Tradewater- “River: Aiki 9 coc eee ee 2,0 

U 
Ulrichye ES OF. ss iri tes 14,21, 23; 39, 43. 5056000 
Unions Comntyso cli eae at he re 2 ee a en ee 42,51, (3, 44 
TID TODS COUNUY, CY 3 eich ce nen ace cpea canescens a eure eee a ere 89 
University. of sCiica eon) = ss. eee EI MER L32yieo 
University<of Michisan Summeroschool 2, eee 109 
Upper? Ohara ge pee ohn eed, core re eee ee ne ee 39 
U.S. GeoloricalsSurvey Ge. eee ee oe , 1,14 

Vee 


Vienna, LIMest one ongiok te cencsscece domes c eee ei ee 71, 87 


INDEX 163 





W. Page 
Vy a ie RT (od oe ee a 21, 31, 42, 55, 61,.64; 69, 78, 100/103 
ko Se a Ae ee oe ee RO ee coe ere 132 
IR RENE Te 0 you ga sa nh agca dor euaig Puree che Miknsceaacadce<EeStavina se suetenscnccte 73 
RE pc RE Se NT RI Gir 2 0 eae a on Se ele 74 
Sena AE DET SPR MMB EE PRECE SS (coc SE. gee oc sG ks bas Suk caaeariscnccocncustetceenenscsadesioeaze 128 
OSU S05 CIC Re 5G a a a BD a Ae 107, 115 
RTI Ck S50 fae a Sor cs korea Parc aPe Senses Si sanneps-=coseacaae= cnc qecenvoksénedabe 113 
SI Er PTL Gh Ua eee ge ae oe RE he cade pcdtdes wacunsuengbncenecunsneasaswcenise iinet 
SeereeeeL TPR SEN COVE CO 51/2 oested 2, cele ck: <cnivad cose ands ead sagvina-selsebicatarconswse 133, 142 
Darernrermrmm roe tt er Cie ye Oa) LCL oes Soo oo 5evearnco-cdecon svecesenne vavteceene-cuacesecebe 11,126 
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